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Carboniferous rocks in the Joggins area, Nova Scotia, and the Maringouin Peninsula, New Brunswick, are world renowned for their well-preserved macroflora, but this paper is the first detailed study of the palynoflora. The section is comprised of the Mississippian Windsor and Mabou groups overlain disconformably by the Lower Pennsylvanian Cumberland...
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... aim of this palynostratigraphic study was to determine the composition of palynomorph assemblages in the upper Viseán, Namurian (Serpukho- vian), and Westphalian (Bashkirian) rocks of the Joggins area, Cumberland depocentre, Nova Scotia, as well as in the nearby upper Viseán and Namurian rocks of Maringouin Peninsula, southeastern New Brunswick ( Figure 1). These data contribute to making palynostratigraphic correlations throughout Atlantic Canada, and provide information concerning the paleoclimate, floral province, and paleoenvironments (at the site of plant growth and at the site of sedimentation). ...
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... locality is situated in the Cumberland depocentre ( Figure 1a) of northwestern Nova Scotia, which is part of the Maritimes Basin ( Gibling 1995). The section, which contains Viseán to Bashkirian rocks, generally dips at moderate angles to the south. ...
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... section, which contains Viseán to Bashkirian rocks, generally dips at moderate angles to the south. Exposures are almost continuous in coastal cliffs, or in the adjacent intertidal areas, from Downing Cove in the northeast, to Shulie in the southwest (Figure 1b) where the succession is interrupted by the Athol and Sand River fault systems. South of these fault systems, excellent exposures continue, but the stratigraphic relationships are difficult to determine. ...
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... formation is 635 m thick. The Joggins Formation, as revised by Calder et al. (2005) and Davies et al. (2005), lies conformably on the Little River Formation and conformably beneath the Springhill Mines Formation at Springhill (Figures 1b and 3). It is 916 m thick ). ...
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... the Joggins coastal section, the Springhill Mines Formation is conformably overlain by the Ragged Reef Formation ( Ryan and Boehner 1994). The latter extends southerly to the vicinity of Shulie (Figures 1b and 4) at which point strata repeat as the coastline projects westerly into Chignecto Bay. Ryan and Boehner (1994) reported a thickness of 667 m for the type section. ...
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... illustrated stratigraphic logs of the main Joggins coastal sections (Figures 7-11) are a composite from several sources. We have relied in part on summary graphic logs published by Ryan and Boehner (1994). ...
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... latter sections, with minor modifications, are those presented by Davies et al. (2005). From the Springhill Mines Formation type section inland at Springhill ( Figures 5 and 11), sampling of coreholes SH-5, SH-74, and SH-99 was guided by graphic logs provided by John Calder (Nova Scotia Department of Natural Resources). In the area south of the Athol and Sand River fault systems ( Figures 6 and 12) we used the measured sections of Salas (1986) supplemented with our own measured section along the southern shore of the Apple River estuary, for the 'Spicers Cove Formation'. ...
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... the Springhill Mines Formation type section inland at Springhill ( Figures 5 and 11), sampling of coreholes SH-5, SH-74, and SH-99 was guided by graphic logs provided by John Calder (Nova Scotia Department of Natural Resources). In the area south of the Athol and Sand River fault systems ( Figures 6 and 12) we used the measured sections of Salas (1986) supplemented with our own measured section along the southern shore of the Apple River estuary, for the 'Spicers Cove Formation'. When our sampling was done, the finely detailed graphic logs of the Little River Formation of Calder et al. (2005) were not yet available, and our samples are plotted adjacent to the log provided by Ryan and Boehner (2004) at that stratigraphic level. ...
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... example, Copeland (1957) studied the arthropod fauna of the Mabou, Cumberland and Pictou groups. He concluded that the interval of nondeposition or erosion of late Namurian age shown by Bell (1944, Figure 10), between the Mabou and lower Cumberland groups of the Southwest Mabou River section of Cape Breton, could not be distinguished on the basis of faunal assemblages and suggested a gradation from the Namurian Mabou Group to the early to middle Westphalian A (Langsettian) strata of the lower Cumberland Group. The latter contains Belinurus refinae Baily, Arthropalaemon dubius (MilneEdwards), and Pygocephalus cooperi Huxley. ...
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... et al. (1960) summarized spore assemblages identified to generic level from the Canso Group (now Mabou Group) and 'Riversdale' Group (now lower Cumberland Group). Five divisions were recognized ( Figure 13). Based partly on the age determinations of the macroflora (Bell 1944) and from the palynological data, they proposed a Namurian A (Serpukhovian) age for the Mabou Group and a Westphalian A (Langsettian) age for the lower Cumberland Group. ...
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... noted the absence of Triquitrites and Vestispora (Foveolatisporites) that are known to occur in overlying formations. Based on correlations with Britain and Belgium, they proposed a Westphalian B (Duckmantian) age ( Figure 13). They also suggested that based on palynological data, the Springhill coal seams were of a similar age to those exposed at Joggins. ...
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... also suggested that based on palynological data, the Springhill coal seams were of a similar age to those exposed at Joggins. This was contrary to the views expressed by some previous Figure 12. Stratigraphic location of samples (bold vertical arrows) from the 'Spicers Cove Formation'. ...
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... present are many of the other genera listed above for the Joggins section coals as well as Cirratriradites, Dictyotriletes, Vestispora (¼Novisporites or Foveolatisporites), and Mooreisporites. They concluded that these beds were early Westphalian C (Bolsovian) ( Figure 13) as they resembled assemblages from the Lonchopteris Zone of the Sydney coalfield. ...
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... preliminary palynological zonation for the uppermost Windsor Group, the Mabou and lower Cumberland groups, that was established by M.S. summarized in Belt (1964 and (Figure 13), was used to support the latter's suggestion that in some localities no disconformity existed between the Mabou and Cumberland groups. Also Belt concluded that inappropriate use of these groups as time stratigraphic units justified their lithostratigraphic revision. ...
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... zonal scheme for the Pictou Group was proposed by Barss and Hacquebard (1967). The group ( Figure 13) contained zones A, B, C, D, and E, which were dated mainly from the macrofloral zones of Bell (1938). Zones A and B were dated as Westphalian C (Bolsovian); Zone C as Westphalian D (Asturian), Zone D as Stephanian and Zone E as Early Permian. ...
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... A and B were dated as Westphalian C (Bolsovian); Zone C as Westphalian D (Asturian), Zone D as Stephanian and Zone E as Early Permian. Neves and Belt (1971) investigated the palynology of samples from immediately above a marine carbonate that they attributed to the uppermost Windsor Group ( Figure 13). They assigned these Hastings Formation beds to the late Viseán. ...
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... example, the Hastings and Pomquet formations were deposited mainly in an arid climate, although it may have been less arid when the upper part of the Pomquet Formation was deposited, whereas humid, coal swamp conditions occurred in possible coeval beds in parts of Britain. Similarly in the Figure 13. Summary of published zonal schemes proposed by previous workers. ...
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... (in Hacquebard 1972, table lV) recognized two zones, a and b/c in the Mabou (Canso) Group, to which he assigned a Namurian (Serpukhovian) age ( Figure 13). The lower Cumberland ('Riversdale') Group contained Zone d of late Namurian age (Bashkirian). ...
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... the Lower Windsor (Arundian to Holkerian) is the Lycospora noctuina var. noctuina-Knoxisporites stephanephorus Zone; in the Upper Windsor (Asbian) Figure 14. Summary of Series and Stages, selected rock units, spore zones, and palynological events. ...
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... (1997) summarized previous work on the palynology of the Carboniferous of Atlantic Canada with special emphasis being placed on the application of palynology to coal geology. Utting and Giles (2004) presented new data from the Windsor and Codroy groups, respectively, of Nova Scotia and Newfoundland (Figures 13 and 14). Correlations were made with the spore zones of Western Europe (e.g. ...
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... total of more than 500 samples was collected from all the localities, and these have been curated at the Geological Survey of Canada (Calgary) for the present palynological study and for possible future work in this and other disciplines. Two-hundred and eleven samples were processed for palynology using standard preparation techniques described by Wood et al. (1996; Figure 1) and most were productive (Figures 15-27). ...
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... total of more than 500 samples was collected from all the localities, and these have been curated at the Geological Survey of Canada (Calgary) for the present palynological study and for possible future work in this and other disciplines. Two-hundred and eleven samples were processed for palynology using standard preparation techniques described by Wood et al. (1996; Figure 1) and most were productive (Figures 15-27). ...
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... occurrence in study area. Lowest part of type section of Shepody Formation, Maringouin Peninsula, New Brunswick (Figures 3, 7, 15); lower part of Shepody Formation, Joggins section, Nova Scotia (Figures 3, 8, 16). comparison of magnetic polarity patterns for the Pomquet Formation (unpublished, work in progress by the authors) with those for the Joggins section reported by Di Venere and Opdyke (1990,1991 As pointed out by other workers such as Nygreen and Bourn (1967) and Ravn (1986), there is continuous morphological transition between pollen assignable to several monosaccate form genera, i.e. ...
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... occurrence in study area. Lowest part of type section of Shepody Formation, Maringouin Peninsula, New Brunswick (Figures 3, 7, 15); lower part of Shepody Formation, Joggins section, Nova Scotia (Figures 3, 8, 16). comparison of magnetic polarity patterns for the Pomquet Formation (unpublished, work in progress by the authors) with those for the Joggins section reported by Di Venere and Opdyke (1990,1991 As pointed out by other workers such as Nygreen and Bourn (1967) and Ravn (1986), there is continuous morphological transition between pollen assignable to several monosaccate form genera, i.e. ...
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... occurrence in study area. Boss Point and Little River formations, Joggins section, Nova Scotia (Figures 3, 16-19). ellipsoides; Potonieisporites elegans, along with the PFWG monosaccate complex are common. ...
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... and geographic occurrence in study area. 'Spicers Cove Formation' in the area south of Sand River, Apple River, Spicers Cove, and the Joggins section, Nova Scotia (Figures 6, 12, 27). ...
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... Pennsylvanian ages shown in the Series and Stages column (Figure 14), are based on those used by many authors, e.g. Gradstein et al. 2004;Heckel and Clayton 2005;Menning et al. 2006. ...
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... these emendations are made, correlations with the British Isles remain tentative, and, even with new Figure 25. Vertical distribution chart of palynomorph taxa in selected samples from the subsurface inland type section of Springhill Mines Formation, Springhill Mines corehole SH-99 (see Figure 11) ordered according to earliest occurrence. Semiquantitative data show relative abundance of taxa. ...
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... 26. Vertical distribution chart of palynomorph taxa in selected samples from the inland type section of Springhill Mines Formation, and lower part of Ragged Reef Formation, Springhill Mines corehole SH-5 (see Figure 11). Taxa occurrences ordered according to earliest occurrence. ...
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... some formations, such as the Goddard Formation of Figure 27. Palynomorph taxa in selected samples of the 'Spicers Cove Formation' in the vicinity of Sand River (section 01 of Salas, 1986); 7 km southwest of Sand River (section 03 of Salas, 1986); Apple River, and Apple River shore sections; Spicers Cove (shore section); (Figure 12). Semi-quantitative data show relative abundance of taxa. ...
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... detailed zonal schemes exist for rocks of the Pennsylvanian of the Illinois Coal Basin (Peppers 1996) and Iowa (Ravn 1986). However, as Peppers Figure 14 for biostratigraphic ages of the zones. Illustrations of selected palynomorphs referred to in the text. ...
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... 1. Selected taxa in Mabou Group. Figure 1. Schopfites claviger Sullivan, 1968, GSC 124291, slide 3, 41.7 6 9.1, GSC loc. ...
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... criteria for determining the ages of the Viseán and early Serpukhovian concurrent range zones found in Plate 2. Selected taxa in Mabou Group. Figure 1. Spelaeotriletes arenaceus Neves and Owens, 1966, GSC 124299, slide 3, 20.5 6 8.9, GSC loc. ...
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... Figure 10. Lophotriletes microsaetosus (Loose) Potonieánd Kremp, 1955, GSC 124308, slide 3, 9.2 6 9.8, GSC loc. ...
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... Figure 11. Apiculatisporis abditus (Loose) , GSC 124309, slide 4, 40.6 6 3.7, GSC loc. ...
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... Figure 12. Acanthotriletes triquetrus Smith and Butterworth, 1967, GSC 124310, slide 3, 25.3 6 11.9, GSC loc. ...
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... Figure 13. Apiculatisporis variocorneus Sullivan, 1964, GSC 124311, slide 3, 31.8 6 4.6, GSC loc. ...
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... Figure 14. Microreticulatisporites nobilis (Wicher) Knox, 1950, GSC 124312, slide 3, 17.95 6 10.72, GSC loc. ...
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... Figure 15. Tricidarisporites arcuatus Neville, in Neves et al., 1973, GSC 124313, slide 3, 31.2 ...
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... Figure 18. Raistrickia saetosa (Loose) Schopf, Wilson, and Bentall, 1944, GSC 124316, slide Atlantic Canada, were previously outlined by Utting and Giles (2004) and von Bitter et al. (2006). ...
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... Figure 19. Raistrickia fulva Artu¨zArtu¨z, 1957, GSC 124317, slide 3, 34.8 6 6.1, GSC loc. ...
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... lack of stratigraphically diagnostic taxa in the R. saetosa Zone, to some extent, explains the different ages attributed by various workers to the base of the Cumberland Group (Figures 13-14) and hence the apparent variations in the duration of the hiatus between the Mississippian and Pennsylvanian. In this paper the base of the zone is somewhat arbitrarily taken as Yeadonian although a Langsettian age can not be ruled out. ...
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Citations
... In eastern Canada, the magnetostratigraphy from the Middleborough Fm ( Figure 12) is inferred to be Brigantian in age based on the late Asbian age for the underlying Limekiln Brook Fm (Giles, 2008;Jutras et al., 2016;Utting et al., 2010). However, since the Limekiln Brook Fm is laterally transitional into the lower part of the Middleborough Fm (Jutras et al., 2016), it is possible that the oldest part of the magnetostratigraphy of Opdyke et al. (2014), consisting of magnetozones NN1-NN2, may extend into the late Asbian rather than being entirely Brigantian ( Figure 12). ...
Plain Language Summary
Nearly synchronous global changes in geomagnetic polarity give both a detailed irregular pacing to geological time and provide a glimpse into heat transfer processes across the core—mantle boundary which drives the Earth's geodynamo. Although the Late Carboniferous is characterized by some well‐studied reversals, details of the tempo of polarity changes in the Early Carboniferous are unknown. This work addresses this by providing a detailed record of polarity changes over a ∼2 million year interval at around 334.5–332.5 million years ago‐from the Trowbarrow Quarry section in NW England. We demonstrate that these limestones likely preserve magnetization from close to their time of formation and record at least 31 polarity reversals. These observations support the idea that the Earth's dynamo was in a hyperactive reversing state similar to those sustained for tens of Myr in the Late Jurassic, parts of the Cambrian and the Late Ediacaran. It further corroborates a ∼200 Myr cyclicity in paleomagnetic field behavior since the Precambrian, potentially linked to variable core heat flow forced by mantle convection.
... Reptiles are a remarkably successful group of tetrapod vertebrates originating in the Carboniferous, about 330 Mya (Didier & Laurin, 2020) that experienced several episodes of diversification throughout their evolutionary history (Sues, 2019). The oldest known reptile, Hylonomus lyelli (Dawson, 1860), lived between 315-320 Mya in what is now Nova Scotia, Canada (Utting et al., 2010;Rygel et al., 2015); however, the Mesozoic is recognised as the 'golden age' of reptiles, with dinosaurs roaming the Earth for nearly 200 Myr. ...
Reptiles represent one of the most diverse groups of tetrapod vertebrates. Extant representatives of reptiles include lepidosaurs (lizards), testudines (turtles) and archosaurs (crocodiles and birds). In particular, they show an important locomotor diversity with bipedal, quadrupedal and facultatively bipedal taxa. This diversity is accompanied by substantial microanatomical disparity in the limb bones. Although many studies have highlighted the link between locomotion and bone microstructure, the latter has never been quantitatively studied from an angular perspective. Indeed, some taxa show microanatomical heterogeneity in cross-section. Here we show, using elliptic Fourier transforms and statistical analyses integrating phylogeny, how angular microanatomical parameters measured on reptilian femoral cross-sections, such as angular bone compactness, can be related to locomotion in this clade. Although phylogeny appears to have a significant impact on our results, we show that a functional signal exists. In particular, we show that bipeds and quadrupeds present a craniolateral-caudomedial and dorsoventral deficit in bone compactness, respectively. This reflects cross-sectional eccentricity in these directions that we relate to the forces acting upon the femur in different postural contexts. This work contributes to deciphering the complex interplay between phylogeny, femoral cross-sectional microanatomy and locomotion in reptiles.
... Reptiles are a remarkably successful group of tetrapod vertebrates originating in the Carboniferous, about 330 Mya (Didier & Laurin, 2020) that experienced several episodes of diversification throughout their evolutionary history (Sues, 2019). The oldest known reptile, Hylonomus lyelli (Dawson, 1860), lived between 315-320 Mya in what is now Nova Scotia, Canada (Utting et al., 2010;Rygel et al., 2015); however, the Mesozoic is recognised as the 'golden age' of reptiles, with dinosaurs roaming the Earth for nearly 200 Myr. ...
Reptiles represent one of the most diverse groups of tetrapod vertebrates. Extant representatives of reptiles include lepidosaurs (lizards), testudines (turtles) and archosaurs (crocodiles and birds). In particular, they show an important locomotor diversity with bipedal, quadrupedal and facultatively bipedal taxa. This diversity is accompanied by substantial microanatomical disparity in the limb bones. Although many studies have highlighted the link between locomotion and bone microstructure, the latter has never been quantitatively studied from an angular perspective. Indeed, some taxa show microanatomical heterogeneity in cross-section. Here we show, using elliptic Fourier transforms and statistical analyses integrating phylogeny, how angular microanatomical parameters measured on reptilian femoral cross-sections, such as angular bone compactness, can be related to locomotion in this clade. Although phylogeny appears to have a significant impact on our results, we show that a functional signal exists. In particular, we show that bipeds and quadrupeds present a craniolateral-caudomedial and dorsoventral deficit in bone compactness, respectively. This reflects cross-sectional eccentricity in these directions that we relate to the forces acting upon the femur in different postural contexts. This work contributes to deciphering the complex interplay between phylogeny, femoral cross-sectional microanatomy and locomotion in reptiles.
... This stratigraphy collectively comprises >3 km of strata that are disconformable on the Mabou Group (Calder et al., 2005;Waldron et al., 2013;Craggs et al., 2017). A series of biostratigraphic (Utting et al., 2010), sedimentological and geochemical studies (Bahr & Keighley, 2021, 2022, have also demonstrated that the overlying >900 m thick strata south of the Anticline, previously described as the Ragged Reef Formation by Ryan et al. (1991), has many similarities to the Grande Anse Formation north of Minudie Anticline, which was first mapped by Norman (1941). The Grande Anse -Ragged Reef formations may have formed as a cover sequence unconformable on older units across the entire Cumberland Basin, or deposition may have been conformable, or disconformable in the Athol Syncline, and gradually onlapped northward across the Minudie Anticline, either way reworking extrusive diapiric material and salt cap-rock into the Black Point sub-basin. ...
Diagenetic models help explain reservoir quality of siliciclastic strata, which are globally important exploration targets for groundwater, petroleum and carbon sequestration. Siliciclastics occur in salt provinces worldwide but remain poorly studied despite documented deviation from basic eodiagenetic models. A new variation is explained based on evidence from Cumberland Basin strata (Grande Anse Formation, Pennsylvanian, Canada). These strata were deposited in a fluvial setting under semi‐humid to humid climates and represent an unconformable cover sequence over a salt wall. Optical microscopy and scanning electron microscopy, both employing cathodoluminescence, reveal that widespread early diagenetic phases are mostly deleterious to reservoir quality. These pre‐compactional eodiagenetic phases are: (i) variable dissolution/alteration of feldspars, micas and carbonate/evaporite clasts; clay and grain staining iron oxides; and pore‐filling kaolinite; (ii) microcrystalline calcite; quartz overgrowths, prismatic quartz, quartzine chalcedony and blocky quartz, the latter two pseudomorphous after gypsum; and barite; (iii) framboidal pyrite and locally extensive Mg, Fe and Mn‐bearing blocky calcite. The first phase is attributed to a seasonally wetted vadose zone under relatively low pH and positive Eh conditions characteristic of humid climates. In contrast, the second phase is usually associated with evaporitic conditions and arid climates, where authigenesis occurs in the capillary fringe to just below the water table, and where porewaters are much more saline. The third phase is related to authigenesis from shallow burial, anoxic, phreatic porewaters. How is the aforementioned humid/arid dichotomy deciphered? Important may be the distinction between vadose and circum‐water‐table phases. Beneath vadose deposits of the humid climate, the proximity of evaporite rock in the salt wall allows for its localized dissolution, providing abundant Ca, CO3 and SO4 ions to produce anomalously saline, shallow groundwater. Barite and transient gypsum precipitated, the latter subsequently replaced by chalcedony and pseudomorphous silica during sporadic events where flushing of meteoric water temporarily lowered pH.
... The fluorite occurs in the outer part of the veins and the barite in the centre. Wider barite veins (with some calcite,~10%) outcrop on the foreshore of Spicer Cove along the fault contact between the Bashkirian (Duckmantian) Ragged Reef Formation [15,16], and Tournaisian Falls Formation conglomerate ( Figure 3). ...
... In addition, one rhyolite from the Squally Point has been analysed ( Figure 5A,B). Spicer Cove along the fault contact between the Bashkirian (Duckmantian) Ragged Reef Formation [15,16], and Tournaisian Falls Formation conglomerate ( Figure 3). Table 1). ...
... The barite at Spicer Cove postdates deposition and deformation of the upper Ragged Reef Formation, dated as late Bashkirian (ca. 314 Ma) [16,30]. The possibility of a much younger age within the Carboniferous or even early Permian cannot be ruled out. ...
Prominent veins of late Carboniferous barite, associated with fluorite and calcite, outcrop close to older granite plutons along an intracontinental shear zone that was active throughout the Carboniferous in southeastern Canada. Some barite is stratigraphically constrained to younger than 315 Ma and final mineralization is constrained by a published Rb–Sr isochron of 300 ± 6 Ma. Barite occurrences in the Carboniferous basins of central Nova Scotia, 50 km to the south, are synchronous with or post-date ankerite-siderite-magnetite-pyrolusite and Pb-Zn mineralization, which was facilitated by fluid interaction with thick evaporites. This study aims to determine controls on the distribution of barite in the shear zone, from field relationships, vein petrography and isotope geochemistry of minerals. The isotope chemistry of shear zone barite is similar to that occurring in Pb-Zn-Mn-Ba mineralization to the south, suggesting a common origin. Veins of barite, associated with fluorite, represent the youngest and regionally coolest phase of a 70 Ma history of Carboniferous mineralized veins along the Minas Fault Zone. Their prominence close to granite plutons reflects brittle deformation of the deeply-rooted granites in a complexly deforming fault zone, but the origin of abundant F remains uncertain.
... To note, both Notalacerta missouriensis and the earliest known reptile, Hylonomus lyelli, come from the same formation and locality (Joggins Formation, UNESCO World Heritage Site, Joggins Fossil Cliffs, Joggins, Nova Scotia, Canada). The Joggins Formation is dated through sporomorphs as early Langsettian/Westphalian A, Bashkirian (e.g., Calder et al., 2006;Utting et al., 2010). No other skeletal records of reptiles are known from the Bashkirian. ...
The origin of Reptilia and the biostratigraphic and palaeobiogeographic distribution of its early representatives are still poorly understood. An independent source of information may come from the extensive Carboniferous footprint record of reptiles, which is arguably richer and more complete than the skeletal record. Nevertheless, previous studies often failed to provide useful information because they were based on poorly preserved material and/or characters non-exclusive of reptile tracks. In fact, a large part of the supposed early reptile tracks can be assigned to the anamniote ichnotaxon Hylopus hardingi. Here, we revise the ichnotaxon Hylopus hardingi based on anatomy-consistent material, attribute it to anamniote reptiliomorphs, and distinguish it from Notalacerta missouriensis, the earliest ichnotaxon that can be attributed to reptiles, and the somewhat younger Varanopus microdactylus (attributed to parareptiles, such as bolosaurians) and Dromopus lacertoides (attributed to araeoscelid reptiles and non-varanodontine varanopids). These attributions are based on correlating morphofunctional features of tracks and skeletons. Multivariate analysis of trackway parameters indicates that the late Bashkirian Notalacerta missouriensis and Hylopus hardingi differ markedly in their trackway patterns from Late Mississippian Hylopus hardingi and Late Pennsylvanian reptile tracks, which appear to share a derived amniote-like type of gait. While the first occurrence/appearance of reptile tracks in the tetrapod footprint record during the late Bashkirian corresponds to the first occurrence/appearance of reptiles in the skeletal record, footprints significantly enlarge the paleobiogeographic distribution of the group, suggesting an earlier radiation of reptiles during the Bashkirian throughout North America and possibly North Africa. Dromopus appeared in the Kasimovian together with the diapsid group Araeoscelidia, but footprints from Western-European occurrences enlarge the paleobiogeographic distribution of diapsids and varanopids. Varanopus and bolosaurian parareptiles appear in the Gzhelian of North America. Older parareptiles are, however, known from the late Moscovian. In all, the footprint record of early reptiles supplements the skeletal record, suggesting possible future lines of research.
... Harvey Lake is underlain by the Kingsclear Group to the northwest and by rhyolite of the Late Devonian Harvey Group to the southeast (Dostal et al., 2016). Red-bed sandstones and mudstones of the Carboniferous Mabou and Pictou groups occur in the southeast of the study area (Ryan et al., 1991;St Peter, 1993;Utting et al., 2010). The Mabou Group comprises fine-grained red-beds with thin interbedded sandstone units overlain by thick units of grey sandstone interspersed with red and grey mudstones (Utting et al., 2010), while the Pictou Group comprises grey or red quartzand feldspar-rich sandstones with a silt or calcite-rich matrix interstratified with red or grey-green mudstones (St Peter, 1993). ...
... Red-bed sandstones and mudstones of the Carboniferous Mabou and Pictou groups occur in the southeast of the study area (Ryan et al., 1991;St Peter, 1993;Utting et al., 2010). The Mabou Group comprises fine-grained red-beds with thin interbedded sandstone units overlain by thick units of grey sandstone interspersed with red and grey mudstones (Utting et al., 2010), while the Pictou Group comprises grey or red quartzand feldspar-rich sandstones with a silt or calcite-rich matrix interstratified with red or grey-green mudstones (St Peter, 1993). Exposed bedrock is commonly weathered to depths of more than 1 m (Balzer and Broster, 1994). ...
The existence of freshwater ferromanganese concretions has been known for decades, but we are not aware of a generally accepted explanation for their formation, and there has been little research into their potential use as records of Holocene climate and paleohydrology. A conceptual model is presented to describe the environmental and geochemical processes which result in the formation and growth of freshwater ferromanganese concretions. In order to evaluate their potential as historical geochemical records, a concretion from Magaguadavic Lake, New Brunswick, Canada is the focus of a detailed geochronological and geochemical investigation. The radiocarbon data provide a coherent growth curve and a maximum age for the concretion of 8448 ± 43 years, consistent with the establishment of Magaguadavic Lake as a stable post-glacial lacustrine system. The data suggest accretion rates of 1.5 and 3.4 mm per 1000 years during the Northgrippian and Meghalayan stages of the Holocene, respectively. The abrupt change in growth rate observed at the stage boundary may be an indicator of Holocene climate change. These features are consistent with inferences from previous research that warmer climate in the Northgrippian led to eutrophication in some lakes in eastern North America. The results confirm that freshwater Fe–Mn concretions may yield important information about past climatic and environmental conditions.
... Early research at Joggins from the mid-1800s to the mid-1900s has been well summarized by Scott (1998), Rygel and Shipley (2005), Calder (2006), and Falcon-Lang (2006). Over the past 25 years, the Joggins Fossil Cliffs have experienced renewed scientific interest, especially in the fields of sedimentology, stratigraphy, and paleobiology, with advancements in paleoenvironmental reconstructions Davies et al. 2005;Rygel et al. 2014) and numerous species discoveries and new taxonomy (Calder 1998;Falcon-Lang 1999, 2003a, 2003b, 2005Falcon-Lang and Bashforth 2004;Utting and Wagner 2005;Calder 2006;Falcon-Lang et al. 2006;Utting et al. 2010;). Grey and Finkel (2011) undertook a review of more recent discoveries and research at Joggins, focusing their interest on the fields of sedimentology and petrology, paleobiology, and paleoenvironmental reconstructions. ...
During the Late Paleozoic Ice Age, the fault-bounded equatorial Cumberland Basin of Nova Scotia experienced rapid subsidence, accumulating kilometer-thick fluvial sedimentary units derived from two highlands to the northwest and southeast. Major variations are recorded in the paleosols exposed at the Joggins Fossil Cliffs, ranging from oxidized and well-drained paleosols with recognizable vertic features to highly reduced organic-rich paleosols. These different soil lithologies suggest alternating conditions between well-drained floodplain environments and water saturation associated with overall poor soil development. Although halokinetic subsidence of the Cumberland Basin is known to have been operative during deposition of these units, previous research favored glacio-eustatic processes as the primary forcing mechanism of sedimentation. A total of 474 fluvial aggradational cycles were identified within a kilometer-thick interval and show a fluctuating accommodation history with a very abrupt nature. The series of fluvial aggradational cycles was used to develop threshold autoregressive models based on 1) their thickness, 2) their paleosol thickness, 3) their sandstone content, and 4) their paleosol-to-sandstone ratio. For each model, results suggest no evidence of statistically significant cyclicity, contradicting the hypothesis that fluvial sedimentation was mainly driven by glacio-eustatic cyclothems. Additionally, a total of 7 lithologies were recognized through 1,655 beds. Evaluation of 8 spherical semivariograms suggests no evidence for cyclicity in the frequency, order, or distribution of the data based on lithologies, although some covariance was found at distances between 550 and 750 m suggesting similar processes controlling sedimentation in the lower and upper Joggins Formation. The Cumberland Basin is known to have been rapidly subsiding, mainly because of ductile deformation of salt deposits in the deeper basinal units. Our results suggest that Joggins records tectonically induced ponding of a part of the sedimentary basin, allowing more extensive preservation of abundant coal and organic-rich units, as well as still-standing fossil forests exposed along the cliffs. These new results suggest that tectonic subsidence of the Cumberland Basin during the Late Paleozoic Ice Age was a more important driver of fluvial sedimentation than previously thought. This novel application of the TAR methodology provides a mathematical description of the sediment accumulation history of terrestrial basins when applied to conformable sedimentary successions, along with the means of linking paleosol development to climatic processes.
... The younger part of this interval is of strong significance, since it is around the base of the Kiaman Superchron, and key polarity marker in the Carboniferous. The age constraining biostratigraphy is largely provided by a miospore zonation, which links it to the British substages, since the two areas were in the same floral province (Utting et al. 2010). A major unconformity separates Mississippian from Pennsylvanian strata (Fig. 12). ...
... A major unconformity separates Mississippian from Pennsylvanian strata (Fig. 12). Whilst the palynostratigraphy has similarity to the European miospore zonations, it also has significant differences, which do not allow the British substage boundaries to be confidently located, but instead provid weaker age equivalence (Utting et al. 2010). ...
The geomagnetic polarity pattern for the Carboniferous is incompletely known, but with the best resolved parts in the Serpukhovian and Bashkirian. Hence, data from both igneous and sedimentary units are also used in an additional polarity bias evaluation. In the Tournaisian to mid Visean interval polarity is mainly derived from palaeopole-type palaeomagnetic studies, allowing identification of polarity bias chrons. Seven polarity bias chrons exist in the Mississippian (MI1n B to MI4n B ) with an additional 33 conventional magnetochrons and submagnetochrons (MI4r to MI9r). The Moscovian and Gzhelian polarity is best resolved in magnetostratigraphic studies from the Donets Basin and the southern Urals. Dispute about the reliability of these data is ill-founded, since an assessment of supporting data from palaeopole-type studies suggests that these datasets currently provide the best magnetic polarity data through the Pennsylvanian. Polarity bias assessment indicates a normal polarity bias zone in the Kasimovian. In the Pennsylvanian there are 27 conventional magnetochrons and submagnetochrons (PE1n to CI1r) and one normal polarity bias chron (PE8n B ). The Kiaman Superchron begins in the mid Bashkirian, with clear data indicating brief normal polarity submagnetochrons within the Superchron. The magnetochron timescale is calibrated using 31 U-Pb zircon dates and a quantitative Bayesian-based age-scaling procedure.
... Notalacerta is the oldest ichnogenus attributed to reptiles and the most abundant reptile track in terms of both number of specimens and number of occurrences during the Pennsylvanian period (e.g., Schneider et al., 2020), therefore an in-depth understanding of its stratigraphic and palaeobiogeographic distribution is central for the understanding of Pennsylvanian tetrapod faunas and to build a meaningful tetrapod footprint biostratigraphy. Due to its notable abundance (it has been recorded in 10 different units/formations, Fig. 10), this ichnotaxon is the reference ichnogenus for the Notalacerta biochron of Fillmore et al. (2012), with the earliest occurrence of the ichnogenus from the early Langsettian site of Joggins, Canada (Joggins Formation; Davies et al., 2005;Utting et al., 2010;Lucas, 2019; this work) (Fig. 10). This coincides with the earliest skeletal record of reptiles (Hylonomus lyelli), occurring at the same site (Dawson 1895, Carroll, 1964, 1988, 2009Reisz 1972;Clack 2002;Calder et al., 2006). ...
The origin of reptiles in the tetrapod footprint record has always been a debated topic, despite the great potential of fossiliferous ichnosites to shed much light on reptile origins when compared to the much less extensive skeletal record. This is in part due to an unclear ichnotaxonomy of the earliest tracks attributed to reptiles that has resulted in unreliable trackmaker attributions. We comprehensively revise the earliest supposed reptile ichnotaxon, Notalacerta missouriensis, based on a neotype and a selection of well-preserved material from the type locality and other sites. A synapomorphy-based track-trackmaker attribution suggests eureptiles and, more specifically, ´protorothyridids´ such as Paleothyris as the most probable trackmakers. A revision of the entire Pennsylvanian-
Cisuralian record of this ichnotaxon unveils an unexpected abundance and a wide palaeogeographical distribution. The earliest unequivocal occurrence of Notalacerta is in the middle Bashkirian (early Langsettian) at the UNESCO World Heritage Site, Joggins Fossil Cliffs (Joggins, Nova Scotia, Canada). This occurrence also coincides with
the earliest occurrence of reptile body fossils (Hylonomus lyelli), which are found at the same site. Notalacerta is abundant and widely distributed during the Bashkirian, mostly in sediments deposited in tidal palaeoenvironments, and less common in the Moscovian and Kasimovian. During the Gzhelian and Asselian, Notalacerta occurrences are unknown, but it occurs again during the Sakmarian and is widespread but not abundant during the Artinskian, mostly in fully continental palaeoenvironments.
