Pub Date : 2020-11-15DOI: 10.3140/bull.geosci.1781
B. Stolfus, B. Cramer, R. Clark, N. Hogancamp, J. Day, S. Tassier-Surine, B. Witzke
coincides with a mass extinction on the scale of the ‘Big Five’ (Sepkoski 1996, Kaiser et al. 2016) and a major perturbation to the global carbon cycle (Cramer et al. 2008, Saltzman & Thomas 2012). The DCB strata of the tri-state area of Missouri, Illinois, and Iowa have been studied for over a century and contain historically important strata for the type Mississippian area including the type area of the lowest Carboniferous North American Kinderhookian Stage (global lower Tournaisian Stage) of the Mississippian Subsystem. The majority of this work occurred more than 50 years ago (e.g., Scott & Collinson 1961) with more recent work limited to the late 1990’s (Chauffe & Nichols 1995, Witzke & Bunker 1996, Chauffe & Guzman 1997). However, significant problems with unit correlation remain due to long standing nomenclature divides across state boundaries, lack of study, or lowresolution sampling. Two units of strikingly similar lithologies, the McCraney Formation and the Louisiana Formation, are critical to the placement of the DCB in the tri-state area. These units often occur within a few miles of one another; however, they have never been identified in the same succession, either in outcrop or in the subsurface. Historically, a nearly equal number of publications have considered these units to be equivalent (e.g., Weller 1900, Weller & Sutton 1940, Harris 1947, Stainbrook 1950) as have considered them to be temporally distinct (Keyes 1895, Weller 1906,
与“五大物种”规模的大规模灭绝(Sepkoski 1996, Kaiser et al. 2016)和全球碳循环的重大扰动(Cramer et al. 2008, Saltzman & Thomas 2012)同时发生。密苏里州、伊利诺伊州和爱荷华州三州地区的DCB地层已经被研究了一个多世纪，其中包含了密西西比子系统石炭世最低北美Kinderhookian阶段(全球下Tournaisian阶段)的密西西比类型地区的重要历史地层。这方面的工作大部分发生在50多年前(例如，Scott & Collinson 1961)，最近的工作仅限于20世纪90年代末(Chauffe & Nichols 1995, Witzke & Bunker 1996, Chauffe & Guzman 1997)。然而，由于长期存在的州界命名分歧、缺乏研究或低分辨率采样，单位相关性仍然存在重大问题。McCraney组和Louisiana组这两个岩性非常相似的单元对于DCB在三州地区的位置至关重要。这些单位经常出现在彼此相距几英里的范围内;然而，无论是在露头还是在地下，它们从未在同一演替中被确定。从历史上看，几乎相同数量的出版物认为这些单位是等效的(例如，Weller 1900, Weller & Sutton 1940, Harris 1947, Stainbrook 1950)，认为它们在时间上是不同的(Keyes 1895, Weller 1906，
{"title":"An expanded stratigraphic record of the Devonian-Carboniferous boundary Hangenberg biogeochemical Event from Southeast Iowa (U.S.A.)","authors":"B. Stolfus, B. Cramer, R. Clark, N. Hogancamp, J. Day, S. Tassier-Surine, B. Witzke","doi":"10.3140/bull.geosci.1781","DOIUrl":"https://doi.org/10.3140/bull.geosci.1781","url":null,"abstract":"coincides with a mass extinction on the scale of the ‘Big Five’ (Sepkoski 1996, Kaiser et al. 2016) and a major perturbation to the global carbon cycle (Cramer et al. 2008, Saltzman & Thomas 2012). The DCB strata of the tri-state area of Missouri, Illinois, and Iowa have been studied for over a century and contain historically important strata for the type Mississippian area including the type area of the lowest Carboniferous North American Kinderhookian Stage (global lower Tournaisian Stage) of the Mississippian Subsystem. The majority of this work occurred more than 50 years ago (e.g., Scott & Collinson 1961) with more recent work limited to the late 1990’s (Chauffe & Nichols 1995, Witzke & Bunker 1996, Chauffe & Guzman 1997). However, significant problems with unit correlation remain due to long standing nomenclature divides across state boundaries, lack of study, or lowresolution sampling. Two units of strikingly similar lithologies, the McCraney Formation and the Louisiana Formation, are critical to the placement of the DCB in the tri-state area. These units often occur within a few miles of one another; however, they have never been identified in the same succession, either in outcrop or in the subsurface. Historically, a nearly equal number of publications have considered these units to be equivalent (e.g., Weller 1900, Weller & Sutton 1940, Harris 1947, Stainbrook 1950) as have considered them to be temporally distinct (Keyes 1895, Weller 1906,","PeriodicalId":9332,"journal":{"name":"Bulletin of Geosciences","volume":"1 1","pages":"469-495"},"PeriodicalIF":1.9,"publicationDate":"2020-11-15","publicationTypes":"Journal Article","fieldsOfStudy":null,"isOpenAccess":false,"openAccessPdf":"","citationCount":null,"resultStr":null,"platform":"Semanticscholar","paperid":"69715917","PeriodicalName":null,"FirstCategoryId":null,"ListUrlMain":null,"RegionNum":3,"RegionCategory":"地球科学","ArticlePicture":[],"TitleCN":null,"AbstractTextCN":null,"PMCID":"","EPubDate":null,"PubModel":null,"JCR":null,"JCRName":null,"Score":null,"Total":0}
Pub Date : 2020-11-15DOI: 10.3140/bull.geosci.1787
D. Botor
mainly determined by the thermal evolution of the basin, which is usually directly related to its burial history. The thermal maturity pattern of the organic matter (degree of coalification, coal rank) is therefore directly related to the burial history of the stratigraphic section analyzed, and the heat transport through the rocks (e.g. Hantschel & Kauerauf 2009). The Intra-Sudetic Basin (ISB) is well-known for its bituminous and anthracite coal deposits occurring in deep, strongly faulted synclines (Kwiecińska 1967; Lipiarski 1976; Mastalerz & Jones 1988; Bossowski 1995; Kwiecińska & Nowak 1997; Nowak 1993, 1996, 1997, 2000; Uglik & Nowak 2015; Pešek & Sivek 2016). Coal was mined in two districts in Poland, Wałbrzych and Nowa Ruda, and in one in the Czech Republic (Žacléř district). Mining operations began in the nineteenth century and the coal mines were all closed by 1999, although there is some potential for further coal and anthracite exploitation. The complicated geological setting (e.g. faults, the steep dips of the upper Carboniferous coal-bearing strata, magmatic events), the abundance of gases (mainly methane and carbon dioxide) and related hazards of methane explosions or gas and rock outbursts, however, make traditional underground coal production uneconomic (Kotarba & Rice 2001; Sechman et al. 2013, 2017). The ISB is a relatively rare case of basin in which a par t icularly high thermal regime resulting from magmatic processes governed a coalification processes. The thermal history and coalification processes of the ISB have, however, seldom been studied (Kułakowski 1979, Mastalerz & Jones 1988, Botor et al. 2020). One of the major products of coalification is methane, and although the coalbed methane reserves in the ISB have not yet been estimated precisely, it might be worthy of exploitation. The distribution and migration of these gases is related to the thermal history of the ISB, and therefore our new findings also contribute to a deeper understanding of this relationship, which might allow for a better prediction of natural gases within sedimentary sequence. The main aim of this study is therefore to improve understanding of the thermal conditions which caused coalification processes in the ISB. This paper is based solely on the kinetic maturity modelling of vitrinite reflectance data which is adopted from previous papers (Chruściel et al. 1985; Bossowski 1997, 2001; Nowak 2000; Ihnatowicz 2001; Botor et al. 2020). The maturity modelling takes into account recent lowtemperature thermochronology results (Sobczyk et al.
{"title":"Burial and thermal history of the Intra-Sudetic Basin (SW Poland) constrained by 1-D maturity modelling - implications for coalification and natural gas generation","authors":"D. Botor","doi":"10.3140/bull.geosci.1787","DOIUrl":"https://doi.org/10.3140/bull.geosci.1787","url":null,"abstract":"mainly determined by the thermal evolution of the basin, which is usually directly related to its burial history. The thermal maturity pattern of the organic matter (degree of coalification, coal rank) is therefore directly related to the burial history of the stratigraphic section analyzed, and the heat transport through the rocks (e.g. Hantschel & Kauerauf 2009). The Intra-Sudetic Basin (ISB) is well-known for its bituminous and anthracite coal deposits occurring in deep, strongly faulted synclines (Kwiecińska 1967; Lipiarski 1976; Mastalerz & Jones 1988; Bossowski 1995; Kwiecińska & Nowak 1997; Nowak 1993, 1996, 1997, 2000; Uglik & Nowak 2015; Pešek & Sivek 2016). Coal was mined in two districts in Poland, Wałbrzych and Nowa Ruda, and in one in the Czech Republic (Žacléř district). Mining operations began in the nineteenth century and the coal mines were all closed by 1999, although there is some potential for further coal and anthracite exploitation. The complicated geological setting (e.g. faults, the steep dips of the upper Carboniferous coal-bearing strata, magmatic events), the abundance of gases (mainly methane and carbon dioxide) and related hazards of methane explosions or gas and rock outbursts, however, make traditional underground coal production uneconomic (Kotarba & Rice 2001; Sechman et al. 2013, 2017). The ISB is a relatively rare case of basin in which a par t icularly high thermal regime resulting from magmatic processes governed a coalification processes. The thermal history and coalification processes of the ISB have, however, seldom been studied (Kułakowski 1979, Mastalerz & Jones 1988, Botor et al. 2020). One of the major products of coalification is methane, and although the coalbed methane reserves in the ISB have not yet been estimated precisely, it might be worthy of exploitation. The distribution and migration of these gases is related to the thermal history of the ISB, and therefore our new findings also contribute to a deeper understanding of this relationship, which might allow for a better prediction of natural gases within sedimentary sequence. The main aim of this study is therefore to improve understanding of the thermal conditions which caused coalification processes in the ISB. This paper is based solely on the kinetic maturity modelling of vitrinite reflectance data which is adopted from previous papers (Chruściel et al. 1985; Bossowski 1997, 2001; Nowak 2000; Ihnatowicz 2001; Botor et al. 2020). The maturity modelling takes into account recent lowtemperature thermochronology results (Sobczyk et al.","PeriodicalId":9332,"journal":{"name":"Bulletin of Geosciences","volume":"1 1","pages":"497-514"},"PeriodicalIF":1.9,"publicationDate":"2020-11-15","publicationTypes":"Journal Article","fieldsOfStudy":null,"isOpenAccess":false,"openAccessPdf":"","citationCount":null,"resultStr":null,"platform":"Semanticscholar","paperid":"42315411","PeriodicalName":null,"FirstCategoryId":null,"ListUrlMain":null,"RegionNum":3,"RegionCategory":"地球科学","ArticlePicture":[],"TitleCN":null,"AbstractTextCN":null,"PMCID":"","EPubDate":null,"PubModel":null,"JCR":null,"JCRName":null,"Score":null,"Total":0}
Pub Date : 2020-11-15DOI: 10.3140/bull.geosci.1799
S. Štamberg
features characterizing species and also fundamentally indicating the individual’s way of life and food selection. The dentition varies considerably depending on the food type and foraging mode (Helfman et al. 2009). The marginal teeth of the maxilla, premaxilla and dentalosplenial can be distinguished from the teeth in the mouth cavity attached to the prearticular and coronoids of the lower jaw and the dermal bones of the palate of the upper jaw and variably on the ventral surface of the parasphenoid. The main function of marginal teeth is to capture and kill prey, retain prey in the mouth, and aid in swallowing. Marginal teeth show great morphological variation. They differ in their size, shape, number and spacing. It is also important to compare the size of the teeth with the size of the skull. Poplin & Heyler (1993) used as an illustration of this ratio a calculation of the tooth height compared to skull depth in front of the opercular series. The species studied in this contribution belong to the group of “primitive” actinopterygians which are characterized by the maxilla and premaxilla being firmly attached to the surrounding dermal bones. Together with the neurocranium, they form a firmly connected unit. Indications of a weakening of this firm connection are only visible in Aeduellidae where there is a regression of the posterior maxillary plate, almost vertical suspensorium and mosaic of small bones in the postorbital area. However, the upper jaw is still firmly attached to the surrounding dermal bones. Mouth open ing is activated by neurocranial elevation and a special mechanism for mandibular depression in all these “primitive” actinopterygians (Schaeffer & Rosen 1961; Lauder 1980, 1982). Schaeffer & Rosen (1961) assumed a fundamentally predaceous feeding mechanism in the “primitive” actinopterygians. Food items were probably caught by biting and swallowed in one piece with participation of the pharyngeal teeth. However, even in primitive actinopterygians, there is a great diversity among the marginal teeth. This diversity includes the probable original arrangement of teeth in two rows with big teeth in the medial row and more numerous smaller teeth in the lateral row (Poplin & Heyler 1993), teeth that are reduced to one row, or teeth that are specialized. Teeth on the dermal bones of the mouth cavity are also
{"title":"Teeth of actinopterygians from the Permo-Carboniferous of the Bohemian Massif with special reference to the teeth of Aeduellidae and Amblypteridae","authors":"S. Štamberg","doi":"10.3140/bull.geosci.1799","DOIUrl":"https://doi.org/10.3140/bull.geosci.1799","url":null,"abstract":"features characterizing species and also fundamentally indicating the individual’s way of life and food selection. The dentition varies considerably depending on the food type and foraging mode (Helfman et al. 2009). The marginal teeth of the maxilla, premaxilla and dentalosplenial can be distinguished from the teeth in the mouth cavity attached to the prearticular and coronoids of the lower jaw and the dermal bones of the palate of the upper jaw and variably on the ventral surface of the parasphenoid. The main function of marginal teeth is to capture and kill prey, retain prey in the mouth, and aid in swallowing. Marginal teeth show great morphological variation. They differ in their size, shape, number and spacing. It is also important to compare the size of the teeth with the size of the skull. Poplin & Heyler (1993) used as an illustration of this ratio a calculation of the tooth height compared to skull depth in front of the opercular series. The species studied in this contribution belong to the group of “primitive” actinopterygians which are characterized by the maxilla and premaxilla being firmly attached to the surrounding dermal bones. Together with the neurocranium, they form a firmly connected unit. Indications of a weakening of this firm connection are only visible in Aeduellidae where there is a regression of the posterior maxillary plate, almost vertical suspensorium and mosaic of small bones in the postorbital area. However, the upper jaw is still firmly attached to the surrounding dermal bones. Mouth open ing is activated by neurocranial elevation and a special mechanism for mandibular depression in all these “primitive” actinopterygians (Schaeffer & Rosen 1961; Lauder 1980, 1982). Schaeffer & Rosen (1961) assumed a fundamentally predaceous feeding mechanism in the “primitive” actinopterygians. Food items were probably caught by biting and swallowed in one piece with participation of the pharyngeal teeth. However, even in primitive actinopterygians, there is a great diversity among the marginal teeth. This diversity includes the probable original arrangement of teeth in two rows with big teeth in the medial row and more numerous smaller teeth in the lateral row (Poplin & Heyler 1993), teeth that are reduced to one row, or teeth that are specialized. Teeth on the dermal bones of the mouth cavity are also","PeriodicalId":9332,"journal":{"name":"Bulletin of Geosciences","volume":"1 1","pages":"369-389"},"PeriodicalIF":1.9,"publicationDate":"2020-11-15","publicationTypes":"Journal Article","fieldsOfStudy":null,"isOpenAccess":false,"openAccessPdf":"","citationCount":null,"resultStr":null,"platform":"Semanticscholar","paperid":"45471143","PeriodicalName":null,"FirstCategoryId":null,"ListUrlMain":null,"RegionNum":3,"RegionCategory":"地球科学","ArticlePicture":[],"TitleCN":null,"AbstractTextCN":null,"PMCID":"","EPubDate":null,"PubModel":null,"JCR":null,"JCRName":null,"Score":null,"Total":0}
Pub Date : 2020-11-15DOI: 10.3140/bull.geosci.1785
Z. Šimůnek, C. Cleal
{"title":"A synopsis of Westphalian‒earliest Stephanian medullosalean and allied plant fossils from the Central and Western Bohemian basins, Czech Republic","authors":"Z. Šimůnek, C. Cleal","doi":"10.3140/bull.geosci.1785","DOIUrl":"https://doi.org/10.3140/bull.geosci.1785","url":null,"abstract":"","PeriodicalId":9332,"journal":{"name":"Bulletin of Geosciences","volume":"1 1","pages":"441-468"},"PeriodicalIF":1.9,"publicationDate":"2020-11-15","publicationTypes":"Journal Article","fieldsOfStudy":null,"isOpenAccess":false,"openAccessPdf":"","citationCount":null,"resultStr":null,"platform":"Semanticscholar","paperid":"44442547","PeriodicalName":null,"FirstCategoryId":null,"ListUrlMain":null,"RegionNum":3,"RegionCategory":"地球科学","ArticlePicture":[],"TitleCN":null,"AbstractTextCN":null,"PMCID":"","EPubDate":null,"PubModel":null,"JCR":null,"JCRName":null,"Score":null,"Total":0}
Pub Date : 2020-08-09DOI: 10.3140/bull.geosci.1778
M. C. Cabral, A. Lord, S. Pinto, L. V. Duarte, A. C. Azerêdo
totype Section and Point (GSSP) for the base of the Toarcian Stage at Peniche, western Portugal (Rocha et al. 2016), all stages of the Early Jurassic are now defined thus providing the essential stratigraphic frame work for developing understanding of global envir onmental conditions and biota for that period of time (201.4–174.2 Ma, Ogg et al. 2016). The Toarcian stage represents a very special phase of Earth history when, to cite Xu et al. (2018, pp. 396–397): “The Toarcian stage (~183–174 Ma) is considered to be the warmest interval of the Jurassic period encompassing a transient temperature rise of up to ~7 °C in mid-latitudes (Dera et al. 2011, Gradstein et al. 2012, Korte et al. 2015). The stage is also marked by one of the most intense and geographically widespread developments of anoxic/euxinic oceanic conditions of the Mesozoic era (Jenkyns 2010). This phenomenon of extreme redox changes is therefore termed the Toarcian Oceanic Anoxic Event (T-OAE, at ~183 Ma) and is marked by large-scale organic-carbon burial in shelf-sea settings, deeper marine basins, and lakes (Jenkyns 1985, 1988; Xu et al. 2017). The T-OAE was characterized by a severe perturbation to the global carbon cycle...”. We give this quotation at length because it is an efficient introduction to Toarcian times, which are currently the subject of a large and rapidly growing literature which it is not our purpose to summarize here. Current work links the growth of a late Pliensbachian cryosphere and its decline in the early Toarcian with climate change and sea level fluctuations, broadly Pliensbachian regression and early Toarcian transgression, and freshwater input into the oceans with greenhouse gases released into the atmosphere and reflected in the carbon isotope record (Ruebsam at al. 2019). This phase of the Earth history also records a widely documented mass extinction (e.g. Hallam 1961, Little & Benton 1995, Caswell et al. 2009, Caruthers et al. 2013, Danise et al. 2013) which is clearly demonstrated in an important group
{"title":"Ostracods of the Toarcian (Jurassic) of Peniche, Portugal: taxonomy and evolution across and beyond the GSSP interval","authors":"M. C. Cabral, A. Lord, S. Pinto, L. V. Duarte, A. C. Azerêdo","doi":"10.3140/bull.geosci.1778","DOIUrl":"https://doi.org/10.3140/bull.geosci.1778","url":null,"abstract":"totype Section and Point (GSSP) for the base of the Toarcian Stage at Peniche, western Portugal (Rocha et al. 2016), all stages of the Early Jurassic are now defined thus providing the essential stratigraphic frame work for developing understanding of global envir onmental conditions and biota for that period of time (201.4–174.2 Ma, Ogg et al. 2016). The Toarcian stage represents a very special phase of Earth history when, to cite Xu et al. (2018, pp. 396–397): “The Toarcian stage (~183–174 Ma) is considered to be the warmest interval of the Jurassic period encompassing a transient temperature rise of up to ~7 °C in mid-latitudes (Dera et al. 2011, Gradstein et al. 2012, Korte et al. 2015). The stage is also marked by one of the most intense and geographically widespread developments of anoxic/euxinic oceanic conditions of the Mesozoic era (Jenkyns 2010). This phenomenon of extreme redox changes is therefore termed the Toarcian Oceanic Anoxic Event (T-OAE, at ~183 Ma) and is marked by large-scale organic-carbon burial in shelf-sea settings, deeper marine basins, and lakes (Jenkyns 1985, 1988; Xu et al. 2017). The T-OAE was characterized by a severe perturbation to the global carbon cycle...”. We give this quotation at length because it is an efficient introduction to Toarcian times, which are currently the subject of a large and rapidly growing literature which it is not our purpose to summarize here. Current work links the growth of a late Pliensbachian cryosphere and its decline in the early Toarcian with climate change and sea level fluctuations, broadly Pliensbachian regression and early Toarcian transgression, and freshwater input into the oceans with greenhouse gases released into the atmosphere and reflected in the carbon isotope record (Ruebsam at al. 2019). This phase of the Earth history also records a widely documented mass extinction (e.g. Hallam 1961, Little & Benton 1995, Caswell et al. 2009, Caruthers et al. 2013, Danise et al. 2013) which is clearly demonstrated in an important group","PeriodicalId":9332,"journal":{"name":"Bulletin of Geosciences","volume":"1 1","pages":"243-278"},"PeriodicalIF":1.9,"publicationDate":"2020-08-09","publicationTypes":"Journal Article","fieldsOfStudy":null,"isOpenAccess":false,"openAccessPdf":"","citationCount":null,"resultStr":null,"platform":"Semanticscholar","paperid":"49078325","PeriodicalName":null,"FirstCategoryId":null,"ListUrlMain":null,"RegionNum":3,"RegionCategory":"地球科学","ArticlePicture":[],"TitleCN":null,"AbstractTextCN":null,"PMCID":"","EPubDate":null,"PubModel":null,"JCR":null,"JCRName":null,"Score":null,"Total":0}
Pub Date : 2020-08-09DOI: 10.3140/bull.geosci.1788
Valentin Jamart, J. Denayer
were located in the southern hemisphere (e.g. Stampfli et al. 2002, 2013; Scotese 2014), with a major mountain range running on the northeastern margin of Laurussia to Gondwana: the Appalachian range (Fig. 1) (DeSantis 2010, Scotese 2014). This period of time is marked by one of the most significant modifications in palaeobiogeography with the precipitated end of the strong faunal endemism of the Emsian–Eifelian and the initiation of the Givetian– Frasnian cosmopolitanism (Oliver & Pedder 1979b). During the early Emsian to late Eifelian interval, three distinct faunal assemblages allow the definition of three different marine realms (Oliver & Pedder 1979a, 1979b, 1994; May 1995, 1997b), separated by various barriers. The Malvinokaffric Realm (MKR), located along the margins of Gondwana (Fig. 1), is relatively poor in corals and it is characterized by cold-water species (Oliver 1990; Oliver & Pedder 1979a, 1979b, 1994; May 1995, 1997b). The East Americas Realm (EAR), located on the eastern part of North America and the northern part of South America (Fig. 1), is characterized by subtropical marine faunas and high degree of endemism (Oliver 1990; Oliver & Pedder 1979a, 1979b, 1994; May 1995, 1997b). The Old World Realm (OWR) covers the Palaeothetys Ocean and the margins of Laurussia, Kazakhstania and Siberia as well as the Chinese blocks and E Australian terranes (Fig. 1). It is also characterized by widespread subtropical marine faunas (Oliver 1990; Oliver & Pedder 1979a, 1979b, 1994; May, 1995, 1997b). The EAR is isolated from the OWR by a continental arch (Fig. 1) and the Appalachian mountain range (Oliver & Pedder 1979a; May 1995, 1997b). Whereas the lowest sea level of the Devonian was recorded during the Emsian (May 1995, 1997b), the Middle Devonian recorded one transgressive pulse. This eustatic increase led to the collapse of the continental arch that separated the EAR from the OWR, and to the opening of a passageway allowing the migration of marine faunas between the two realms (Oliver & Pedder 1979a, DeSantis & Brett 2011). The faunal turnovers observed in the EAR are a probable consequence of this major
{"title":"The Kačák event (late Eifelian, Middle Devonian) on the Belgian shelf and its effects on rugose coral palaeobiodiversity","authors":"Valentin Jamart, J. Denayer","doi":"10.3140/bull.geosci.1788","DOIUrl":"https://doi.org/10.3140/bull.geosci.1788","url":null,"abstract":"were located in the southern hemisphere (e.g. Stampfli et al. 2002, 2013; Scotese 2014), with a major mountain range running on the northeastern margin of Laurussia to Gondwana: the Appalachian range (Fig. 1) (DeSantis 2010, Scotese 2014). This period of time is marked by one of the most significant modifications in palaeobiogeography with the precipitated end of the strong faunal endemism of the Emsian–Eifelian and the initiation of the Givetian– Frasnian cosmopolitanism (Oliver & Pedder 1979b). During the early Emsian to late Eifelian interval, three distinct faunal assemblages allow the definition of three different marine realms (Oliver & Pedder 1979a, 1979b, 1994; May 1995, 1997b), separated by various barriers. The Malvinokaffric Realm (MKR), located along the margins of Gondwana (Fig. 1), is relatively poor in corals and it is characterized by cold-water species (Oliver 1990; Oliver & Pedder 1979a, 1979b, 1994; May 1995, 1997b). The East Americas Realm (EAR), located on the eastern part of North America and the northern part of South America (Fig. 1), is characterized by subtropical marine faunas and high degree of endemism (Oliver 1990; Oliver & Pedder 1979a, 1979b, 1994; May 1995, 1997b). The Old World Realm (OWR) covers the Palaeothetys Ocean and the margins of Laurussia, Kazakhstania and Siberia as well as the Chinese blocks and E Australian terranes (Fig. 1). It is also characterized by widespread subtropical marine faunas (Oliver 1990; Oliver & Pedder 1979a, 1979b, 1994; May, 1995, 1997b). The EAR is isolated from the OWR by a continental arch (Fig. 1) and the Appalachian mountain range (Oliver & Pedder 1979a; May 1995, 1997b). Whereas the lowest sea level of the Devonian was recorded during the Emsian (May 1995, 1997b), the Middle Devonian recorded one transgressive pulse. This eustatic increase led to the collapse of the continental arch that separated the EAR from the OWR, and to the opening of a passageway allowing the migration of marine faunas between the two realms (Oliver & Pedder 1979a, DeSantis & Brett 2011). The faunal turnovers observed in the EAR are a probable consequence of this major","PeriodicalId":9332,"journal":{"name":"Bulletin of Geosciences","volume":"95 1","pages":"279-311"},"PeriodicalIF":1.9,"publicationDate":"2020-08-09","publicationTypes":"Journal Article","fieldsOfStudy":null,"isOpenAccess":false,"openAccessPdf":"","citationCount":null,"resultStr":null,"platform":"Semanticscholar","paperid":"44051554","PeriodicalName":null,"FirstCategoryId":null,"ListUrlMain":null,"RegionNum":3,"RegionCategory":"地球科学","ArticlePicture":[],"TitleCN":null,"AbstractTextCN":null,"PMCID":"","EPubDate":null,"PubModel":null,"JCR":null,"JCRName":null,"Score":null,"Total":0}
Pub Date : 2020-08-09DOI: 10.3140/bull.geosci.1767
V. Turek, Š. Manda
no typic characters in ectocochleate cephalopods. The origin and biological function of colour patterns is a matter of ongoing discussions and wellfounded data concerning its evolution are still very limited (Williams 2017). However, the poor knowledge on colour patterns in fossil ectocochleate cephalopods significantly increased in the last decades (Mapes & Davis 1996, Turek & Manda 2011, Mapes & Larson 2016). Colour patterning of the nautiloid shell was studied in relation to animal phenotype, autecology, habitat and taphonomy; the applicability for nautiloid taxonomy was discussed (Ruedemann 1921, Foerste 1930a, Kobluk & Mapes 1989, Mapes & Davis 1996, Manda & Turek 2009a). Up to now, colour patterns are documented in 47 early Palaeozoic nautiloid species (for a list with references, see Tab. 1). We have not regarded those species, in which colour patterns were mentioned (Foerste 1930a, Strids berg 1985) but neither illustrated nor described in detail (see Turek 2009). Colour patterns in Early Palaeozoic nautiloids have been recorded in representatives of the orders Oncocerida, Discosorida, (both subclass Multiceratia), Tarphycerida and Nautilida, while colour patterning in evolutionary older Cambrian and Early Ordovician nautiloids is still unknown. The vast majority of species displaying colour patterns belong to the order Oncocerida possessing straight or slightly curved breviconic shells (Barrande 1865–1870, Foerste 1930a). Colour patterns in oncocerids with coiled or almost straight shell were documented in only a few cases (Manda & Turek 2009a, Turek 2009). Oncocerids display a high disparity of their shell form, ranging from straight, slowly expanding to coiled, trochoceraconic forms (Sweet 1964, Dzik 1984, Manda & Turek 2009b), which is linked to the disparity in colour patterns. The colour patterning in Multiceratia includes longitudinal and
{"title":"Discontinuous, asymmetric and irregular colour patterns in Silurian oncocerids (Nautiloidea) with cyrtoconic shells","authors":"V. Turek, Š. Manda","doi":"10.3140/bull.geosci.1767","DOIUrl":"https://doi.org/10.3140/bull.geosci.1767","url":null,"abstract":"no typic characters in ectocochleate cephalopods. The origin and biological function of colour patterns is a matter of ongoing discussions and wellfounded data concerning its evolution are still very limited (Williams 2017). However, the poor knowledge on colour patterns in fossil ectocochleate cephalopods significantly increased in the last decades (Mapes & Davis 1996, Turek & Manda 2011, Mapes & Larson 2016). Colour patterning of the nautiloid shell was studied in relation to animal phenotype, autecology, habitat and taphonomy; the applicability for nautiloid taxonomy was discussed (Ruedemann 1921, Foerste 1930a, Kobluk & Mapes 1989, Mapes & Davis 1996, Manda & Turek 2009a). Up to now, colour patterns are documented in 47 early Palaeozoic nautiloid species (for a list with references, see Tab. 1). We have not regarded those species, in which colour patterns were mentioned (Foerste 1930a, Strids berg 1985) but neither illustrated nor described in detail (see Turek 2009). Colour patterns in Early Palaeozoic nautiloids have been recorded in representatives of the orders Oncocerida, Discosorida, (both subclass Multiceratia), Tarphycerida and Nautilida, while colour patterning in evolutionary older Cambrian and Early Ordovician nautiloids is still unknown. The vast majority of species displaying colour patterns belong to the order Oncocerida possessing straight or slightly curved breviconic shells (Barrande 1865–1870, Foerste 1930a). Colour patterns in oncocerids with coiled or almost straight shell were documented in only a few cases (Manda & Turek 2009a, Turek 2009). Oncocerids display a high disparity of their shell form, ranging from straight, slowly expanding to coiled, trochoceraconic forms (Sweet 1964, Dzik 1984, Manda & Turek 2009b), which is linked to the disparity in colour patterns. The colour patterning in Multiceratia includes longitudinal and","PeriodicalId":9332,"journal":{"name":"Bulletin of Geosciences","volume":"1 1","pages":"333-367"},"PeriodicalIF":1.9,"publicationDate":"2020-08-09","publicationTypes":"Journal Article","fieldsOfStudy":null,"isOpenAccess":false,"openAccessPdf":"","citationCount":null,"resultStr":null,"platform":"Semanticscholar","paperid":"41898942","PeriodicalName":null,"FirstCategoryId":null,"ListUrlMain":null,"RegionNum":3,"RegionCategory":"地球科学","ArticlePicture":[],"TitleCN":null,"AbstractTextCN":null,"PMCID":"","EPubDate":null,"PubModel":null,"JCR":null,"JCRName":null,"Score":null,"Total":0}
Pub Date : 2020-08-09DOI: 10.3140/bull.geosci.1793
M. Mergl
Four types of dendritic microborings preserved as natural casts were observed on the surfaces of brachiopod shells from the Silurian in Central Bohemia: Rhopalondendrina jakubinka isp. nov., ? Clionolithes isp., and an indeterminate dendrinid are of Llandovery (Aeronian) age, Clionolithes amoebae isp. nov. is of Ludlow (Gorstian) age. Rhopalondendrina jakubinka forms a dense plexus of thin rhizoidal tunnels extending from a broad and curved entrance tunnel. ? Clionolithes isp. forms characteristically rarely branching thin meandering tunnels with a globular central node, while C. amoebae forms rosette-like microborings with sinuously curved primary branches and scarce lateral branches of smaller size. Microborings are present both on outer and inner surfaces of shells; their location and number confirm massive infestation of dead shells which were exposed on the sea floor for long time intervals and which were not affected by mechanical abrasion of the shells. This indicates narrow ecological limits for these endobionts, most likely within the deeper euphotic zone.
{"title":"Dendritic microborings in brachiopod shells from the Silurian of the Barrandian area, Czech Republic","authors":"M. Mergl","doi":"10.3140/bull.geosci.1793","DOIUrl":"https://doi.org/10.3140/bull.geosci.1793","url":null,"abstract":"Four types of dendritic microborings preserved as natural casts were observed on the surfaces of brachiopod shells from the Silurian in Central Bohemia: Rhopalondendrina jakubinka isp. nov., ? Clionolithes isp., and an indeterminate dendrinid are of Llandovery (Aeronian) age, Clionolithes amoebae isp. nov. is of Ludlow (Gorstian) age. Rhopalondendrina jakubinka forms a dense plexus of thin rhizoidal tunnels extending from a broad and curved entrance tunnel. ? Clionolithes isp. forms characteristically rarely branching thin meandering tunnels with a globular central node, while C. amoebae forms rosette-like microborings with sinuously curved primary branches and scarce lateral branches of smaller size. Microborings are present both on outer and inner surfaces of shells; their location and number confirm massive infestation of dead shells which were exposed on the sea floor for long time intervals and which were not affected by mechanical abrasion of the shells. This indicates narrow ecological limits for these endobionts, most likely within the deeper euphotic zone.","PeriodicalId":9332,"journal":{"name":"Bulletin of Geosciences","volume":"1 1","pages":"319-332"},"PeriodicalIF":1.9,"publicationDate":"2020-08-09","publicationTypes":"Journal Article","fieldsOfStudy":null,"isOpenAccess":false,"openAccessPdf":"","citationCount":null,"resultStr":null,"platform":"Semanticscholar","paperid":"44993207","PeriodicalName":null,"FirstCategoryId":null,"ListUrlMain":null,"RegionNum":3,"RegionCategory":"地球科学","ArticlePicture":[],"TitleCN":null,"AbstractTextCN":null,"PMCID":"","EPubDate":null,"PubModel":null,"JCR":null,"JCRName":null,"Score":null,"Total":0}
Pub Date : 2020-08-09DOI: 10.3140/bull.geosci.1765
Erik Tihelka, L. Tian, C. Cai
With over 6,600 described species, harvestmen represent a morphologically and ecologically diverse group of arachnids with a cosmopolitan distribution. Although members of the order Opiliones are believed to have been among some of the earliest terrestrial arthropods, the Palaeozoic fossil record of harvestmen is sparse. Herein, a new harvestman, Devonopilio hutchinsoni gen. et sp. nov., is described based on a penis preserved in Lower Devonian Rhynie chert from Aberdeenshire, Scotland (Pragian, ca. 407 Ma). Together with Eophalangium sheari , another Early Devonian harvestman known from the Rhynie chert, the new species represents the earliest member of the order Opiliones in the fossil record and one of the oldest terrestrial animals. The new species differs significantly from E. sheari in penis morphology, indicating that harvestmen began to diversify before the Early Devonian. Devonian harvestman
已描述的种类超过6600种，是一种形态和生态多样化的蜘蛛纲动物，分布在世界各地。尽管Opiliones目的成员被认为是最早的陆生节肢动物之一，但古生代收割机的化石记录却很少。在此，一个新的收割机，Devonopilio hutchinsoni gen. et sp. nov.，是基于保存在苏格兰阿伯丁郡下泥盆世Rhynie chert (Pragian，约407 Ma)的阴茎来描述的。这一新物种与另一种早泥盆纪的收获动物——雷尼燧石的Eophalangium sheari一起，代表了化石记录中最早的Opiliones目成员，也是最古老的陆生动物之一。该新种在阴茎形态上与sheari E.有显著差异，表明收割机在早泥盆世之前就开始多样化了。德文郡的收割者
{"title":"A new Devonian harvestman from the Rhynie chert (Arachnida: Opiliones)","authors":"Erik Tihelka, L. Tian, C. Cai","doi":"10.3140/bull.geosci.1765","DOIUrl":"https://doi.org/10.3140/bull.geosci.1765","url":null,"abstract":"With over 6,600 described species, harvestmen represent a morphologically and ecologically diverse group of arachnids with a cosmopolitan distribution. Although members of the order Opiliones are believed to have been among some of the earliest terrestrial arthropods, the Palaeozoic fossil record of harvestmen is sparse. Herein, a new harvestman, Devonopilio hutchinsoni gen. et sp. nov., is described based on a penis preserved in Lower Devonian Rhynie chert from Aberdeenshire, Scotland (Pragian, ca. 407 Ma). Together with Eophalangium sheari , another Early Devonian harvestman known from the Rhynie chert, the new species represents the earliest member of the order Opiliones in the fossil record and one of the oldest terrestrial animals. The new species differs significantly from E. sheari in penis morphology, indicating that harvestmen began to diversify before the Early Devonian. Devonian harvestman","PeriodicalId":9332,"journal":{"name":"Bulletin of Geosciences","volume":" ","pages":""},"PeriodicalIF":1.9,"publicationDate":"2020-08-09","publicationTypes":"Journal Article","fieldsOfStudy":null,"isOpenAccess":false,"openAccessPdf":"","citationCount":null,"resultStr":null,"platform":"Semanticscholar","paperid":"43065227","PeriodicalName":null,"FirstCategoryId":null,"ListUrlMain":null,"RegionNum":3,"RegionCategory":"地球科学","ArticlePicture":[],"TitleCN":null,"AbstractTextCN":null,"PMCID":"","EPubDate":null,"PubModel":null,"JCR":null,"JCRName":null,"Score":null,"Total":0}
Pub Date : 2020-05-30DOI: 10.3140/bull.geosci.1771
R. Morga
indices of thermal maturity of pre-Upper Silurian rocks, in which vitrinite does not appear (e.g. Goodarzi 1984, 1985; Goodarzi & Norford 1985, 1987, 1989; Link et al. 1990; Cole 1994; Petersen et al. 2013; Luo et al. 2020). It is commonly employed in the recognition of the unconventional hydrocarbon deposits, which frequently occur in the Cambrian–Silurian organic-rich shales (e.g. Więcław et al. 2010, Schovsbo et al. 2011, Jarvie 2012, Petersen et al. 2013). However, the chemical structure of the graptolite periderm (or fusellum sensu Maletz et al. 2014) is still not fully resolved. Periderm of living graptolites was composed of collagen-like fibrils but their corresponding fossil counterparts lack protein and they underwent the coalification process similar to plant remains (Towe & Urbanek 1972, Link et al. 1990). Deep insight into graptolite paleobiology was given by Maletz et al. (2017). Research on the chemistry of the fossilized graptolite periderm (Bustin et al. 1989; Suchý et al. 2002, 2004; Caricchi et al. 2016; Morga & Kamińska 2018; Luo et al. 2020) were mostly performed on graptolite specimens, reflectance (Rr) of which exceeded values of 0.8–1%, and still little is known about chemistry of low reflectance graptolites. The purpose of this investigation is to determine, for the first time, chemical properties of the graptolite periderms from the Holy Cross Mountains (Rr < 0.8%), and compare them to those known from the previous studies. The research is a continuation of the microstructural examination performed on the same samples (Morga 2019).
{"title":"Chemical properties of the graptolite periderm from the Holy Cross Mountains (Central Poland)","authors":"R. Morga","doi":"10.3140/bull.geosci.1771","DOIUrl":"https://doi.org/10.3140/bull.geosci.1771","url":null,"abstract":"indices of thermal maturity of pre-Upper Silurian rocks, in which vitrinite does not appear (e.g. Goodarzi 1984, 1985; Goodarzi & Norford 1985, 1987, 1989; Link et al. 1990; Cole 1994; Petersen et al. 2013; Luo et al. 2020). It is commonly employed in the recognition of the unconventional hydrocarbon deposits, which frequently occur in the Cambrian–Silurian organic-rich shales (e.g. Więcław et al. 2010, Schovsbo et al. 2011, Jarvie 2012, Petersen et al. 2013). However, the chemical structure of the graptolite periderm (or fusellum sensu Maletz et al. 2014) is still not fully resolved. Periderm of living graptolites was composed of collagen-like fibrils but their corresponding fossil counterparts lack protein and they underwent the coalification process similar to plant remains (Towe & Urbanek 1972, Link et al. 1990). Deep insight into graptolite paleobiology was given by Maletz et al. (2017). Research on the chemistry of the fossilized graptolite periderm (Bustin et al. 1989; Suchý et al. 2002, 2004; Caricchi et al. 2016; Morga & Kamińska 2018; Luo et al. 2020) were mostly performed on graptolite specimens, reflectance (Rr) of which exceeded values of 0.8–1%, and still little is known about chemistry of low reflectance graptolites. The purpose of this investigation is to determine, for the first time, chemical properties of the graptolite periderms from the Holy Cross Mountains (Rr < 0.8%), and compare them to those known from the previous studies. The research is a continuation of the microstructural examination performed on the same samples (Morga 2019).","PeriodicalId":9332,"journal":{"name":"Bulletin of Geosciences","volume":" ","pages":""},"PeriodicalIF":1.9,"publicationDate":"2020-05-30","publicationTypes":"Journal Article","fieldsOfStudy":null,"isOpenAccess":false,"openAccessPdf":"","citationCount":null,"resultStr":null,"platform":"Semanticscholar","paperid":"45258159","PeriodicalName":null,"FirstCategoryId":null,"ListUrlMain":null,"RegionNum":3,"RegionCategory":"地球科学","ArticlePicture":[],"TitleCN":null,"AbstractTextCN":null,"PMCID":"","EPubDate":null,"PubModel":null,"JCR":null,"JCRName":null,"Score":null,"Total":0}
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