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The coal-bearing strata of the Lower Cretaceous Mannville Group (Western Canadian Sedimentary Basin, South Central Alberta), PART 2: Factors controlling the composition of organic matter accumulations
Accepted Manuscript The coal-bearing strata of the Lower Cretaceous Mannville Group (Western Canadian Sedimentary Basin, South Central Alberta), part 2: Factors controlling the deposition of organic matter accumulations
Silvia Omodeo Salé, Rémy Deschamps, Pauline Michel, Benoit Chauveau, Isabel Suárez-Ruiz PII: DOI: Reference:
S0166-5162(17)30095-2 doi: 10.1016/j.coal.2017.05.020 COGEL 2847
To appear in:
International Journal of Coal Geology
Received date: Revised date: Accepted date:
2 February 2017 30 May 2017 31 May 2017
Please cite this article as: Silvia Omodeo Salé, Rémy Deschamps, Pauline Michel, Benoit Chauveau, Isabel Suárez-Ruiz , The coal-bearing strata of the Lower Cretaceous Mannville Group (Western Canadian Sedimentary Basin, South Central Alberta), part 2: Factors controlling the deposition of organic matter accumulations. The address for the corresponding author was captured as affiliation for all authors. Please check if appropriate. Cogel(2017), doi: 10.1016/j.coal.2017.05.020
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ACCEPTED MANUSCRIPT The Coal-bearing strata of the Lower Cretaceous Mannville Group (Western Canadian Sedimentary Basin, South Central Alberta), Part 2: Factors controlling the deposition of organic matter accumulations.
Silvia OMODEO SALÉ1 , Rémy DESCHAMPS1 , Pauline MICHEL1 , Benoit
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CHAUVEAU1 and Isabel SUÁREZ-RUIZ2
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(1) IFPEN, 1 & 4 Avenue du Bois-Préau, 92852 Rueil-Malmaison cedex – France
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(2) INCAR – CSIC, c./ Francisco Pintado Fe, 26, 33011 Oviedo - Spain
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Corresponding author: [email protected]
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Abstract
This work analyzes the distribution of coal-bearing strata in the stratigraphic framework of the
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Mannville Group (Lower Cretaceous, Western Canada Sedimentary Basin). In the 3rd -order depositional sequence the maximum abundance of coal layers is found in the highstand system
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tracts (HST), whereas in the 4th -order eustatic sequences, coal deposits distribute similarly in the highstand and transgressive system tracts (TST). These trends have been related to the variation
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of accommodation space in the basin, which mostly influence the occurrence of favorable conditions for organic matter preservation. Petrographic analyses permit to identify variation in the coal layers composition and to relate them with the stratigraphic dynamic of the basin. The HST is characterized by a low subsidence rate, which induces low levels of the groundwater table, favoring dry conditions in the peat. By consequence, in the HST a higher abundance of inertinite maceral group is observed than in the TST. On the other hand, the TST is characterized by higher subsidence rates, thus more stable groundwater table levels, promoting the organic matter preservation. Therefore, in the TST a higher content of vitrinite and liptinite maceral groups is observed. In correspondence of the
ACCEPTED MANUSCRIPT maximum flooding surface (MFS), the peat is frequently flooded, with the consequent dilution of the organic matter with terrigeneous sediment, forming carbonaceous shales deposits. By the analysis of the organic matter composition, seven depositional environments for coal were identified, located at different distance from the coast line. Each depositional environment is characterized by a specific organo-facies association, which is the reflex of different
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environmental conditions in the peat, in terms of water table level, type of vegetation and hydrodynamic processes. The vertical superimposition in a coal package of different
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depositional environments has been related to high order climatic cyclicity (5th -order
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transgressive and regressive cycles), which controls the groundwater table fluctuations.
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Highlights
Distribution of the coal deposits in the stratigraphic framework
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The organic matter preservation is controlled by the accommodation space The depositional environments where coal forms are defined
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High order climatic cyclicity induces compositional changes in the coal beds
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Keywords: coal; macerals analysis; petrographic index; Mannville Group; accommodation
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space; groundwater table
1. INTRODUCTION Accumulation of organic matter can be found in a very large variety of depositional environments, from continental to marine. However, only in few cases the environmental conditions are favorable for the preservation in the sediment of great amount of organic matter to form coal deposits and/or hydrocarbons source rocks (Bordenave, 1993; Taylor et al., 1998). Different types and amount of organic matter can be deposited, depending on the type of producers, the proximity to the coastline, the river drainage, the redox conditions of the depositional environment and the residence time in the degradation zone (including oxidation reactions but also reduction processes) (Arthur and Sageman, 1994; Berner and Canfield, 1989;
ACCEPTED MANUSCRIPT Bralower and Thierstein, 1984; Burdige, 2007; Tyson, 2001). This work aims to improve the understanding of the formation of deposits containing abundant organic matter, which form in the alluvial to the coastal-tidal plains depositional settings. These deposits have a relevant economic interest, because they can form coal deposits and gas-prone source rocks (carbonaceous shales mostly formed by Type III kerogen). Thus, understanding the processes of
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formation, distribution and composition variation of these types of rocks in the basin is of great scientific and economic interest. To achieve the objective proposed in this work, the coal beds
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forming the Mannville Group deposits (Lower Cretaceous, Western Canada Sedimentary Basin,
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Alberta, Canada) were analyzed.
The conditions required to form carbonaceous rocks are mainly: 1) the presence of important
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sources of organic matter during deposition and 2) the setting of favorable condition for organic matter preservation during the geological history of the basin (Taylor et al., 1998). The
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preservation of the coal layers is strictly controlled by the position of the water table relative to the surface, which is influenced by the accommodation rate, the eustatic variations and the
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rainfall rate in the peat (Banerjee et al., 1996; Bohacs and Suter, 1997; Holz et al., 2002). The groundwater table level controls the degree of humidity in the soil, thus the type of vegetation
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produced and accumulated and the diagenetic gelification processes. The combination of these factors determines the organo-facies characterizing the coal deposits (e.g. Banerjee et al., 1996; Cross, 1988; Chalmers et al., 2013; Diessel et al., 2000; Flint et al., 1995; Gastaldo et al., 1993;
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Teichmüller and Teichmüller, 1982; Wadsworth et al., 2002, 2003). Hydrologic regimes characterized by low water level determine frequent oxidation and degradation of the organic matter formed in the peat, whereas very high groundwater levels can drown the mire and favors the deposition of relevant amounts of terrigeneous sediments. At the equilibrium point favorable conditions for the accumulation and the preservation of high content of well-preserved and structured organic matter (Diessel et al., 2000). A relationship between the environmental conditions of the ancient peat-forming ecosystems and the petrological composition of the organic matter preserved have been extensively inferred in the literature (e.g. Calder et al., 1991; Cohen et al., 1987; Chalmers et al.,
ACCEPTED MANUSCRIPT 2013; Davies et al., 2005; Diessel, 1982, 1986; Diessel et al., 2000; Diessel, 1992, 2007; Harvey and Dillon, 1985; Holz et al., 2002; Stach et al., 1982; Staub, 2002; Styan and Bustin, 1983; Teichmüller, 1989; Wadsworth et al., 2003; Wadsworth et al., 2010). Diessel (1982) was the first to propose a method to describe the organo-facies composition in coals, based on the definition of petrographic indices. The most relevant indices considered are i) the tissue
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preservation index (TPI) and ii) the gelification index (GI). The TPI index provides an indication of the presence of structured or unstructured materials and thus of the type of
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vegetation dominant in the peat. The GI index gives an indication of the humidity in the peat
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and thus of the degree of the dryness and of the groundwater table level. The petrographic indices proposed have been used to reconstruct facies diagrams (Diessel, 1986), where each
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field represents the combination of specific environmental conditions. Diessel’s indices were used, modified and integrated by several authors (e.g., Calder et al., 1991; Nicolas et al., 1997;
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Petersen, 1993), improving the interpretation of the environmental conditions where TOM forms in different geological contexts and areas.
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In the past, several studies have been specifically carried out to link the maceral composition of the Mannville Group coal deposits with the paleo-environments of the peat
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where they have been formed (Kalkreuth and Leckie, 1989; Kalkreuth et al., 1991; Lamberson et al., 1991; Marchioni and Kalkreuth, 1991), with the main scope to differentiate the compositional characteristics of the coal formed in the strandplain in respect to the delta plain
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settings. Herein, the sub-depositional environments where the Mannville Group coal deposits formed are analyzed in detail, by means of organo-facies analysis and the interpretation of petrographic indices. The distribution of these sub-depositional environments in the stratigraphic framework was also determined, trying to understand the link between coal composition with the groundwater table fluctuation, which is in turn related to the interaction among the different orders transgressive/regressive cyclicities.
2. GEOLOGICAL SETTING
ACCEPTED MANUSCRIPT The Western Canada Sedimentary Basin (WCSB) is a northeast-southwest major clastic wedge of the foreland basin derived from the Cordillera. It extends from the Cordillera foreland thrust belt towards the Canadian Shield and it covers an area of approximately 2 million km2 (Fig. 1). The thickness of the wedge reaches its maximum at the east of the foothills front, at the axis of the Alberta Syncline (about 6000 meters) and it decreases in the northeast direction,
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towards the Canadian Shield (Strobl, 1988). The infill of the WCSB resulted from two tectonic phases (Cant and Abrahamson, 1996). In the first Paleozoic-Jurassic phase, it formed a
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succession dominated by carbonate sedimentation and deposited on the top of the stable craton,
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next to North America's earlier passive margin. In a second mid-Jurassic-Paleocene phase, a context of foreland basin was instated. The foreland succession overlaid the previous carbonate
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deposits and mainly consists of clastic deposits, coming from uplifted Canadian Cordillera. Following these two successions, during the Paleocene, net erosion and sediment by-pass have
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prevailed in the area. In the second tectonic phase, as the North American plate started to drift westward with the opening of the Atlantic ocean, the western margin of the continent suffered at
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least two major compression episodes, which led to uplift of thrusted and folded rocks that formed the Canadian Rocky Mountains. As a consequence of this tectonic activity, the foreland
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was subject to two distinct subsidence phases, from Late Jurassic (Oxfordian) to Early Cretaceous and from the Middle Cretaceous (Aptian) to Eocene, separated by a major unconformity (Cant and Abrahamson, 1996). The Mannville Group was deposited on these
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unconformities, overlying tilted and truncated strata ranging from the Paleozoic to the Mesozoic Eras (Cant and Abrahamson, 1996; Jackson, 1984). The Mannville Group deposited during Barremian-Aptian to Early Albian Stage (+/- 120 to 104 My) and it blanketed the entire Western Canadian foreland basin, with a thickness ranging from less than 40 meters eastward to more than 700 meters in the Rocky Mountain Foothills. In the study area (Fig. 1) thickness ranges from 95 to 320 meters (Hayes et al., 1994). The entire Group corresponds to a third-order sequence (Cant and Abrahamson, 1996), bordered at the top and at the bottom by tectonically generated unconformities. The Lower Mannville strata corresponds to the lowstand system tract (Jackson, 1984) and it consists of fluvial sediments
ACCEPTED MANUSCRIPT that change upward into marginal marine deposits (estuarine to tidal and shoreface deposits) and are sealed by offshore marines shales corresponding to the maximum flooding surface (MFS) of the same order sequences (Cant and Abrahamson, 1996; Langenberg et al., 1997). The latter transgressive deposits are considered as part of the informal “Middle Mannville”. The Upper Mannville deposits correspond to the highstand system tract (Jackson, 1984) and it is a
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succession of shallow marine sediments that progressively change into fluvial, coastal plain and floodplain facies. The Upper Mannville encompasses a set of successive progradations across
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the whole basin, in a northward direction. Generally marine shale deposits are found in the
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north, shoreface sandstones in the central part of the basin and continental deposits are deposited in the south (Cant and Abrahamson, 1996). In the entire Manville Group several coal
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deposits have been identified, with a maximum abundance in the Upper Mannville. Coal layer extended throughout the entire basin, with lateral extension up to more than 300 km and vertical
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thickness from 1 to 10 meters.
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3. METHODOLOGY
Eight cores representative of the Middle-Upper Mannville Group deposits were selected
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(Fig. 2). These cores represent the stratigraphic record of eight wells located along the geological cross-sections reconstructed by Deschamps et al., (in press). The stratigraphic record of each core was described by means of facies analysis and it was subdivided in 4 th -order
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depositional sequences, with definition of the related lowstand (LST), transgressive (TST) and highstand (HST) system tracts (Fig. 3). To determine the features of the Mannville Group coal deposits, a total of 106 samples were collected, each one representing a single point in the cores (Table 1) and analyzed by means of petrographic and geochemical analyses. Samples were formed by both coal (Carbon content, C >50%) and carbonaceous shales (C <50%). To quantify the relative abundance of the coal in the 4th -order system tracts, the cumulative thickness of the coal measured in the HST, TST and LST system tract, forming each depositional sequence, in respect to the total cumulative coal thickness measured in the total
ACCEPTED MANUSCRIPT core was determined (Table 2). To normalize this data, for each system tract, the proportion of the coal cumulative thickness relative to the total sediment thickness was also determined.
3.1. Petrographic Analyses The petrographic analyses were performed at the Petrography laboratory of the INCAR
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(Oviedo, Spain). Petrographic pellets were prepared for petrographic analysis according to the standard procedure described in the ISO-7404-2 (2009) norms. The maceral analysis was
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carried out on the coal and shaly coal samples (formed by dispersed organic matter – DOM),
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based on 500 counts per sample (Appendix 1). The analysis was performed using reflected MPV-Combi-Leitz optical microscope with an oil immersion objective (50x) and with a point-
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counter coupled to the microscope. Incident white light was used, together with fluorescence mode when necessary, after excitation with UV and blue-violet light under a Leica DM 4500P
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microscope. Maceral analysis determines the relative proportion of the macerals in the sample. Mineral matter was included in the count. Maceral classification was determined according to
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the (ISO-7404-2, 2009) norms and using the last established maceral classification defined in ICCP (1998; 2001), Sýkorová et al. (2005) and Pickel et al. (2016).
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The results of the maceral analysis were used to calculate petrographic indices proposed in the literature (Diessel, 1986; Kalkreuth and Leckie, 1989) (see Table 3 for indices explication and Appendix 2 for indices results). Petrographic indices provide information on: 1) the
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humidity rate in the peat (SF/F, T/F, and GI indices); 2) the vegetation type (ligneous or herbaceous) (W/D, S/D, TPI and VI indices); 3) the intensity of the degradation/preservation processes (Vs/Vd, IR and S/D indices) and 4) the influence of the groundwater table (V/I and GWI) (Table 3). Indices were calculated only on the samples containing more than 50% of organic carbon. In the case of the samples formed by carbonaceous shales petrographic indices were not determined, because organic matter fragments were too small for maceral classification. Thus, only the proportions of vitrinite, inertinite and liptinite maceral groups were defined for these samples. The integration of the data provided by the different indices permits to describe the environmental conditions prevailing at the time of peat accumulation.
ACCEPTED MANUSCRIPT To reconstruct the depositional environments where the organic matter accumulated, the facies diagram proposed by Diessel (1986) and modified by Nicolas et al. (1997) was used. In this diagram variations of the TPI (tissue preservation index) and GI (gelification index) indices (Diessel, 1986) identify 6 fields, each one representing different environmental conditions of the peat, in terms of humidity rate, frequency of the groundwater table oscillations, type of
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vegetation and preservation/degradation processes. The combination of these properties defines specified organic matter depositional environments. Thus, an organic matter depositional
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environment was determined for each sample. In the case of the samples whose indices were
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projected in the intersection of the fields of two depositional environments, both depositional
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environments were considered (Fig. 4).
Proximate and Ultimate Analyses
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Moisture, ash, and volatile matter contents were obtained (Appendix 3), according to the ASTM-D7582-10 (1981) and ISO-562 (1998) standards. For the same subset of samples, the C,
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H, N, and total sulfur contents were determined using a LECO CHN 2000 and a LECO S632 apparatus, according to the ASTM-D5373-08 (2008) and ASTM-D4239-08 (2008). Analyses
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were carried out on samples crushed to less than 212 µm. The determination of C and Ash discerns coal (C > 50%) from the shaly coal and coaly shale deposits (C < 50%), formed by
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dispersed organic matter (DOM) in the mineral matrix.
4. RESULTS
4.1. Thickness and properties of the coal layers in the 4 th-order eustatic sequences The frequency of occurrence of the coal layers in the 4th -order eustatic sequences and the proportion of the coal thickness in respect to the total thickness of each system tract was calculated for the eight cores (Table 2). The average of the values obtained for the eight cores indicate that the 51% of the coal layers formed in the HST, the 46% in the TST and the 3% in the LST. In several cases the maximum flooding surface (MFS) of the 4 th -order eustatic sequences, which marks the transition between the TST and the HST, passes throughout the
ACCEPTED MANUSCRIPT coal layers. The coal deposits form the 19% of the total system tract thickness in the HST and the 17% in the TST. Coal layers have an average thickness of nearly 1 meter in both system tracts. In the case of the LST, frequency was not calculated, as there is only one data point. A synthesis of the petrographical and geochemical characteristics of the coal layers formed in the different 4th -order system tracts is presented in Table 4. Data were obtained calculating
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the average of the values measured, by proximate and ultimate Analyses and maceral analysis, in the samples forming part of each system tract. Samples collected in correspondence of the
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MFS were considered separately. The content of organic carbon (C) is similar in the coal layers
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composing the HST (56%) and the TST (45%). The lowest content of C (%) is measured in the samples collected at the MFS (average of 24%), as herein mostly form dispersed organic matter
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deposits (DOM). The highest contents of ST are measured in the samples formed in the TST (2.5%).
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The petrographic composition of the coal deposits was determined considering the average percentage of the three maceral groups (vitrinite, inertinite and liptinite) counted in the samples
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representing each 4th -order system tract (Table 4). Mineral matter-free data indicate that the vitrinite is the most abundant maceral group in both TST and HST (53% and 66% respectively).
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The inertinite maceral group is more abundant in the HST (40%) than in the TST (27%) and the liptinite maceral group is more abundant in the TST (9%). The highest content of mineral matter is found in the layers formed in correspondence of the MFS (61%), which in most of the case
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constitute carbonaceous shales. A higher content of mineral matter is contained in the coal deposits formed in the TST (31%) than in the HST (19%).
4.2. Definition of higher order cycles in the coal packages Centimetric to metric packages of coal can be found along the entire Upper Mannville Group stratigraphic record. Petrographic observations evidence relevant differences in terms of maceral composition in the samples collected in a same package. The calculation of petrographic indices helped to describe and to understand these variations (Table 3). Vs/Vd, IR, W/D, S/D, TPI and VI indices >1 generally indicate a good preservation of the vegetal tissues
ACCEPTED MANUSCRIPT and the dominance of forest vegetation, whereas lower values (< 1) indicate a poor preservation of the vegetal tissues and the dominance of swamp, marsh and grass vegetation (Diessel, 1986; Kalkreuth and Leckie, 1989). High SF/F, T/F and GI indices suggest wet conditions in the peat, whereas low values indicate dry conditions. High Vs/Vd, IR and S/D indices indicate a good preservation of the organic matter, whereas low values suggest a degraded and bracket state
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(Diessel, 1986; Kalkreuth and Leckie, 1989). Variations of the petrographic indices along a same package (Fig. 2 and Appendix 2) allow
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high order cycles (5th order) to be individually identified (Fig. 3), which can correspond to
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regressive and transgressive events induced by high order climatic oscillations (Chalmer et al., 2013, Wadsworth et al., 2010). Deepening cycles (DP) are generally formed by organic matter
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which petrographic indices indicate the dominance in the peat of wet conditions (high SF/F, T/F and GI indices), the presence of vegetation formed by arborescent plants (Vs/Vd, IR, W/D, S/D,
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TPI and VI indices >1) and good preservation conditions (high Vs/Vd, IR and S/D indices). The shallowing cycles (SH) are represented by organic matter whose petrographic indices indicate
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drier conditions in the peat (low SF/F, T/F and GI indices), the dominance of shrub, grass and detrital vegetation type (Vs/Vd, IR, W/D, S/D, TPI and VI indices <1) and relevant oxidation
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and degradation of the organic matter (low Vs/Vd, IR and S/D indices). Passing from the SH to the DP cycles, an increase of the mineral matter content was frequently observed (Fig. 2 and
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Appendix 2).
4.3. Coal depositional environments Plotting the TPI (Tissue Preservation Index, rate between the structured and unstructured macerals) and the GI (Gelification Index, rate between gelified and oxidized macerals) indices on the facies diagram proposed by Diessel (1986) and modified by Nicolas et al. (1997) (Fig. 4), the environmental conditions where the peat forms are defined for each sample (Fig. 3). High TPI values indicate large amount of well-preserved plant tissues and are interpreted to reflect the abundance of arboreal vegetation (wood-derived macerals). Low TPI values indicate higher degradation of the organic matter and relevant contribution of detrital woody matter. High GI
ACCEPTED MANUSCRIPT indicates high humidity rate in the peat, due to high groundwater table levels, which allows the gelification processes to develop extensively. On the contrary, low GI values indicates dryer conditions, which favored the oxidation of the organic matter. The combination of these indices permits identification of six coal depositional environments: Terrestrial, Dry Forest, Wet Forest, Swamp Forest, Limnic and Reed Moor. An additional depositional environment was proposed
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herein (Open Moor), describing a limnotelmatic setting where shaly coal and coaly shale formed (C < 50%) (Wadsworth et al., 2010). In this latter depositional environment mixed terrestrial
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and marine organic matter deposited.
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The distribution of the proposed depositional environments in the alluvial and coastal plains is shown in Fig. 5. The environmental conditions and the preservation processes dominating in
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these settings were constraint interpreting the petrographic indices and the microscopic features
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observed. A synthetic overview of those environments is given in Figs. 6-9 and Table 5.
4.4. Occurrence of the coal depositional environments in the stratigraphic framework
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The percentage frequency of occurrence of the defined coal depositional environments in the 4th -order system tracts was determined (Fig. 10). In the case for a same samples the TPI and
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GI indices were projected in the intersection of two fields, both depositional environments were counted. Therefore, the sum of the frequency of distribution of the seven depositional environments defined is nearly higher than 100% (Fig. 10).
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The Terrestrial and Dry Forest depositional environments form mostly in the HST; the Wet Forest and Swamp Forests depositional environments in the TST and at the TST-HST transition, in correspondence of the MFS; the Reed Moor depositional environment forms mostly in the HST; the Limnic depositional environment in the TST and in correspondence of the MFS; the open moor forms mostly in the MFS and secondarily in the TST. Therefore, in the HST form with higher frequency the Terrestrial, the Dry Forest and the Reed Moor depositional environments (Fig. 10). In the TST a more uniform distribution of the coal depositional environments is observed. The Terrestrial and Dry Forest depositional environments are the less
ACCEPTED MANUSCRIPT represented. The samples collected at the MFS are formed mostly in the Open Moor depositional environment (Fig. 10).
5. DISCUSSION 5.1. Coal deposits in the stratigraphic framework
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The variation of the accommodation space in the terrestrial setting is expressed by the fluctuation of the groundwater table, which in turn is induced by the different orders regressive
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and transgressive cycles recorded in the basin (Bohacs and Suter, 1997; Wadsworth et al., 2002,
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2003). At the 3rd -order cyclicity, the most numerous coal layers form in the highstand system tract (HST) and particularly in the early to middle part (Fig. 2) (Deschamps et al., in press). At
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this time the rising of the groundwater table is stable low enough for favoring vertical and lateral peat accumulation (Bohacs and Suter, 1997, Wadsworth et al., 2003). Differently, at the
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4th -order cyclicity, coal distributes with similar proportion and layer thickness in the TST and in the HST (Table 2). This observation is confirmed by the proportion of the coal layers in respect
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to the total thickness of sediments, which indicate the preservation of similar abundance of organic matter in both HST and TST (Table 2). This different trend, in respect to what was
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observed in the 3rd -order depositional sequences, may be the consequence of the lower variation of the accommodation space at 4th -order, which permits to maintain favorable condition for organic matter preservation in both HST and TST. By contrast, very little organic matter is
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observed in the 4th -order LST, suggesting that at this stage the accommodation rate was generally lower than the production rate, with consequent lower groundwater table levels, favoring the erosion of the peat and avoiding the preservation of the organic matter. The geochemical signal of the organic matter formed and preserved in the 4th -order HST and TST is very similar (Table 4). The only relevant difference is the proportion of total sulfur content (evaluated in %), which is contained in higher proportion in the TST (Appendix 3). This trend can be related to the influence of sea-water during the transgressive periods (high sea level), which favored the formation of pyrite in the peat.
ACCEPTED MANUSCRIPT Variation in the organic matter composition is detected by petrographic analyses. A relationship between the type of organic matter accumulated in the peat and the eustatic and accommodation space cycles has been proposed in the literature (Banerjee et al., 1996; Chalmers et al., 2013; Davies et al., 2005; Diessel et al., 2000; Wadsworth et al., 2002, 2003). The regressive and transgressive cycles have a direct influence on the hydrologic regimes
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(groundwater table oscillations), which determine variation in the environmental conditions in the peat and thus of the organic matter accumulated. In the 4th -order eustatic sequences of the
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Mannville Group high content of the inertinite maceral group is measured in the HST (Table 4),
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indicating the dominance in this eustatic regime of dry and oxidized environmental conditions in the peat. The latter may be a consequence of the low accommodation space formed in the
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HST, which determine low levels and/or high fluctuation of the groundwater table. On the other hand, in the TST the vitrinite maceral is very abundant and well preserved, and it is frequently
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associated with liptinite. This composition reflects the maintenance in the transgressive periods of high water levels of the groundwater table, which favors the gelification and preservation of
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the organic matter and the deposition of aquatic origin (rich in lipids). At the MFS dominate the formation of carbonaceous shales, as very high levels of the groundwater table are reached,
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determining the “long-term” drowning of the mire and the deposition of relevant amounts of terrigeneous sediments.
Maceral analysis reveals high organic-facies heterogeneity along package of organic matter
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rich-deposits formed in a same cycle (Fig. 3). This heterogeneity can be observed at very low scale (deci-metric to cent-metric) and it is evidenced by variation of the petrographic indices (Appendix 2).
The distribution of the petrographic indices along the stratigraphic record indicates a cyclicity in the organo-facies associations and thus in the environmental conditions of the peat. Therefore, it can be suggested that the variation of the organo-facies associations in a same package is induced by high order eustatic/climatic cyclicity (5th order or higher) that determines the shift of the coast line during the time and the oscillation of the groundwater table. The latter determines variation over time of the humidity rate and thus on the vegetation type and on the
ACCEPTED MANUSCRIPT gelification/oxidation processes. Similarly to what was observed in the 4th -order eustatic sequences, 5th -order shallowing-regressive cycles are associated with organo-facies association of dry conditions and frequent exposition of the peat, whereas in the deepening-transgressive cycles organo-facies indicative stable wet conditions.
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5.2. Formation of the coal depositional environments The maceral associations found in an organic matter-rich layer are related to the
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characteristics of the depositional setting where it was deposited. Therefore organo-facies have
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been associated with specific sub-depositional environments that form in the alluvial and deltatidal plains (Calder et al., 1991; Cohen et al., 1987; Chalmers et al., 2013; Davies et al., 2005;
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Diessel, 1982, 1986; Diessel et al., 2000; Diessel, 1992, 2007; Harvey and Dillon, 1985; Holz et al., 2002; Stach et al., 1982; Staub, 2002; Styan and Bustin, 1983; Teichmüller, 1989;
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Wadsworth et al., 2003; Wadsworth et al., 2010). These sub-depositional environments are located at different distance from the coast-line, which determines a different dynamic of the
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precipitation, evaporation and infiltration processes. The combination of these parameters is reflected in the groundwater table level, which in turn determines the rate of humidity in the
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peat and thus the type of vegetation (Bohacs and Suter, 1997; Moore and Shearer, 2003). The oscillation of the groundwater table influences also the preservation state of the organic matter, as
frequent
fluctuations
cause
the
exposition
and
oxidation
of
the
peat.
The
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preservation/degradation of the organic matter in the peat is additionally related to the energy of the fluvial, tidal and waves processes, which determines the intensity of the transport and the erosion of the organic matter and also the supply in the peat of terrigeneous material. The energy of the depositional setting is strictly linked to the position along the sedimentary profile. Therefore the position where it is located the peat in the alluvial-delta plain, determine the type of organic matter deposited (Fig. 5). The Terrestrial depositional environment is located in the most alluvial plain landward position (Fig. 5). At this point, frequent oscillations of the groundwater table are suggested, which cause continuous exposition of the peat. Thus, organic matter can be easily reworked by
ACCEPTED MANUSCRIPT meteoric agents and by fluvial transportation, giving as result a high fragmentation and oxidation of the vegetal tissues, frequently mixed with relevant amount of mineral matter (Fig. 6a-d). In the distal part of the alluvial part forms the Dry Forest depositional environment. In this environment the organic matter is well preserved and it is formed mostly by high plant remains (Fig. 6e-h). Thus, in respect to the Terrestrial depositional environment, a groundwater
PT
table more stable and a lower energy conditions are suggested for this environment, which permit the development of a high plants forest. However, the high oxidation of the organic
SC
conditions, thus of low levels of the groundwater table.
RI
matter (Fig. 6g and h) indicates the dominance also in this depositional environment of dry
In the proximal part of the upper delta plain forms the Wet Forest depositional environment
NU
(Fig. 5). In this environment organic matter is very well preserved and formed mostly by high plant tissues. Thus, a stable and relatively high level of the groundwater table is suggested,
MA
which favors the gelification and preservation of the organic matter (Fig. 7a-d). In the seaward position of the upper delta plain forms the Swamp Forest depositional environment (Fig. 5). In
ED
this environment the organic matter is formed mostly by remains of shrub vegetation, whereas high plants decrease. The abundance of aquatic-affinity macerals (e.g. alginite) and the
EP T
abundant mineral matter alternated with the organic matter (Fig. 7e-h), indicate more aquatic conditions in respect to the previous depositional environment. Thus, higher level of the groundwater table is suggested.
AC C
In the lower delta plain and in the interdistributary fluvial channels areas, the Reed Moor depositional environment (Fig. 5) is formed. The organic matter formed in this environment is mostly made up of shrub and grass vegetation remains, whereas high plants rest are less common. The increased energy in this part of the sedimentary profile of the tide, fluvial and wave currents makes unfavorable the development of high plants vegetation. In this environment, strong fluctuations of groundwater table occurred, which determine alternation of dry and wet condition and of exposition and flooded of the peat (Fig. 8a-d). In the delta plain shallow lakes, ponds and other aqueous environments from freshwater to hypersaline can be formed. In these environments forms the Limnic depositional environment (Fig. 5),
ACCEPTED MANUSCRIPT characterized by a stable and high groundwater table.. Swamp/shrub vegetation and aquaticaffine organic matter dominates, whereas high plants do not frequently develop. The organic matter is frequently alternated with terrigeneous material (Fig. 8e-h), which indicates a periodic flooding of the peat. In the distal part of the lower delta plain, close to the coast line, the Open Moor depositional
PT
environment can be formed (Fig. 5). This environment is characterized by a constant very high level of the groundwater table, which determines a continuous and relevant input of terrigenous
RI
material in the peat (Fig. 9). In the low energy areas, conditions favorable for organic matter
SC
deposition can be cyclically replaced with flooded events, with a high terrigeneous sediment supply, forming deposits constituting by alternation of organic matter and mineral matter layers
NU
(Fig. 9a-d). In these deposits, aquatic organic components (mostly algae) are frequent (Fig. 9d and h). On the other hand, in the high energy areas, accumulation of organic matter fragments,
MA
included in a mineral matter matrix, can be formed (Fig. 9e-h). In the Open Moor depositional environment abundant pyrite is found (Fig. 9e), suggesting the proximity of the sea.
ED
The distribution of the coal depositional environments in the stratigraphic framework is strictly related to the dynamic of the groundwater table. The regressive periods are characterized
EP T
by low subsidence and by the shift of the coast line seaward. Thus, the formation of a reduced accommodation space and the low level of the groundwater table favour the formation in the 4th order HST of depositional environments located in the landward position and characterized by
AC C
dry conditions (Terrestrial and Dry Forest depositional environments) (Fig. 10). On the other hand, in the transgressive periods, the higher subsidence and the shift of the coast line landward permit the formation of high accommodation space and high level of the groundwater table. Therefore in the 4th -order TST the depositional environments characterized by wet conditions (Wet Forest, Swamp Forest, Limnic and Open Moor) are more frequently found (Fig. 10). Due to the high accommodation space of the transgressive periods, large fluctuations of the groundwater table are possible, which determines the setting of a larger variability of depositional environments (from Terrestrial to Open Moor) (Fig. 5).
ACCEPTED MANUSCRIPT The results presented in this work allows the characteristics of the organic matter deposited in a basin to be related to the factors that influence the stratigraphic evolution of a basin and the features of the related depositional settings, which are, among others: the accommodation space, the sediment supply, the climate, the precipitation and evaporation rate, the type of vegetation and the primary production. This type of data is necessary when wanting to predict the
PT
distribution and preservation of the organic matter in a stratigraphic framework of a basin. The results obtained herein represent the basis for future works that aim to model the deposition of
SC
RI
the terrestrial organic matter in a basin.
6. CONCLUSIONS
NU
The analysis of the Mannville Group stratigraphic record provides relevant data on the distribution of the coal and carbonaceous shales in the stratigraphic framework of a sedimentary
MA
basin and on the variation of its compositional and geochemical properties. A relevant condition to preserve the coal deposits in a sedimentary basin is the achievement of
ED
the equilibrium between the accommodation and the peat production rate. In the 3rd -order depositional sequence this equilibrium is reached in the early-middle highstand, where form the
EP T
thickest and more laterally continuous coal layers. In the 4th -order depositional sequences, coal deposits distribute similarly in the highstand and transgressive system tracts, indicating that equilibrium conditions were equally reached in these periods.
AC C
In the 4th -order depositional sequences, very similar geochemical properties were observed between the organic matter formed in the TST and HST. However, some relevant differences are determined by means of petrographic analyses. The inertinite maceral group is more abundant in the HST, indicating the dominance of drier conditions and low levels of the groundwater table. The liptinite maceral group is more abundant in the TST, as the groundwater table reaches high levels, favoring the deposition of aquatic macerals rich in lipids. The variation of the environmental conditions in the peat determines the great heterogeneity of the relative abundance of the macerals constituting the organic matter. These variations are induced by 5th -order cycles, which oscillation causes the shift of the coast line along the
ACCEPTED MANUSCRIPT sedimentary profile, determining variation in the humidity rate, the type of vegetation and the fluvial to coastal transportation and hydrodynamic processes in the peat. The combination of these elements are expressed by the variation of the groundwater table level, which can be considered as one of the most relevant factor controlling the organo-facies (maceral association) forming the coal deposits.
PT
In the alluvial to delta plain organic matter accumulates in different depositional environments, each one characterized by specific environmental conditions and thus, different organo-facies
RI
association. The environmental conditions characterizing each depositional environment are
SC
strictly related with the dynamic of the groundwater table and with the energy of the environment, which in turn are influenced by the different order regressive/transgressive cycles
NU
and from the distance from the coast-line. In the HST of the 4th -order depositional sequences occurred with more frequency the depositional environments characterized by dry conditions
MA
(Terrestrial, Dry Forest and Reed Moor), thus low levels of the groundwater table. On the other hand, in the TST dominate the depositional environments characterized by wet conditions (Wet
ED
Forest, Swamp Forest and Limnic), thus higher levels of the groundwater table. The larger variability in the TST is due to the higher accommodation space formed in this period, which
EP T
permits higher fluctuation of the groundwater table and, thus, the formation of different depositional environmental conditions. This study demonstrates that the prediction of the terrestrial organic matter signature at a basin-scale cannot be considered only through the
AC C
depositional settings, whereas it is necessary to take into account the dynamic of the groundwater table, which is in turn induced by regressive and transgressive cycles, thus related to local tectonic events and to climatic external forcing.
Acknowledgements This paper is part of a larger IFPEN research project, dedicated to the stratigraphic modelling of organic matter distribution at basin scale (DORS project). Authors would like to thank INCARCSIC (Oviedo, Spain) for providing lab equipment and material for the petrographic and
ACCEPTED MANUSCRIPT geochemical analyses. Finally we thank the two IJCG reviewers, whom revisions and suggestions have considerably improved the quality of the manuscript. Appendix 1 – Maceral analysis data
Well/ sample
Depth (m)
T elinit Collot Vitrodet Collo Corpo Geli Sporin Cutini Resini e elinite rinite detrini gelilin nite inite te te t. te
Subei nite.
Algini Liptodet Bitum Fusini Semifusi te rinite inite te nite
10-25-40-25W4 1.0
9.5
0.0
31.9
0.0
0.0
4.2
0.2
11
1559
7.3
0.4
0.0
27.4
0.0
0.0
2.3
0.0
10
1559.2
0.8
1.2
0.0
27.3
0.0
0.2
1.0
0.2
9
1559.6
0.0
6.8
0.6
14.6
0.0
0.4
2.6
0.2
1560
0.6
13.7
0.2
50.5
0.0
0.0
1.9
7
1560.5
10.4
8.2
0.0
45.3
0.0
0.0
1.2
6
1571.5
0.0
28.9
5.0
0.8
0.0
0.0
5
1573.9
0.6
4.9
2.2
2.4
0.0
0.0
4
1574.2
1.6
50.8
0.2
35.0
0.0
0.0
3
1574.6
0.4
10.7
0.2
28.8
0.0
0.0
2
1575
0.4
8.1
0.0
62.7
0.0
0.0
1
1575.8
0.4
49.1
0.8
22.6
0.0
0.2
1122.2
0.0
28.7
2.0
14.6
0.0
23
1127
0.4
24.7
0.6
40.3
22
1132.1
3.7
20.0
1.2
16.5
21
1132.45
17.5
9.4
19
1146.4
0.0
2.6
20
1146.8
0.2
23.6
18
1146.9
0.0
3.0
17
1149.35
12.5
18.7
16
1167.4
0.0
15
1167.8
0.0
14
1168.1
13
1168.6
0.0
0.0
31.7
1.3
0.0
0.0
0.0
0.4
0.0
0.0
0.4
0.0
5.0
42.2
0.0
12.2
50.3
0.2
0.0
0.0
0.4
0.0
6.4
31.4
0.0
0.6
0.0
0.0
1.2
0.0
0.0
0.0
0.0
4.0
18.9
0.0
0.0
0.0
5.3
23.7
0.0
0.0
0.0
0.2
1.4
0.0
0.0
1.0
0.2
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.8
0.6
0.8
0.6
0.0
0.0
0.0
0.0
0.4
6.0
NU
5.2
1.4
0.0
0.2
0.0
0.0
0.4
0.0
6.3
38.9
3.6
0.0
0.4
0.0
0.0
1.0
0.0
4.6
13.2
2.0
0.0
0.2
0.0
0.0
1.0
0.0
1.8
8.1
0.0
9.0
0.0
0.0
0.0
1.2
1.2
0.0
0.6
8.4
0.2
2.3
7.5
1.0
0.8
0.0
0.2
0.8
0.0
3.4
13.0
2.2
0.4
2.2
0.0
0.0
0.0
0.0
0.0
0.0
3.3
13.9
2.2
18.7
33.5
0.4
0.0
1.8
0.2
2.5
0.0
0.0
1.8
0.0
0.0
0.0
0.0
31.2
0.0
0.0
0.0
0.0
1.6
0.4
2.8
2.2
0.2
0.0
3.0
0.2
0.0
0.0
0.0
0.0
0.0
0.0
1.6
0.4
0.0
0.0
12.9
0.0
0.0
0.0
4.2
1.8
1.0
0.4
1.4
0.0
28.0
0.4
0.5
5.3
0.0
1.5
0.0
0.4
2.5
0.0
1.3
16.0
2.2
1.8
31.6
0.0
0.2
0.0
0.4
0.2
0.0
0.0
0.0
0.0
3.4
34.4
2.4
1.6
11.6
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
16.2
17.5
1.3
27.4
0.4
0.2
4.8
0.0
0.0
0.0
0.0
0.6
0.0
3.1
17.7
2.2
7.4
39.1
0.2
0.2
7.4
0.2
0.2
0.0
0.0
1.4
0.0
7.0
26.7
EP T
ED
0.0
12.6
1.2 0.0
34.4
0.0
1170
0.0
9.3
6.3
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
11
1170.5
7.2
55.0
5.2
17.4
0.8
0.8
0.0
0.4
0.0
0.0
0.2
0.0
0.0
0.0
4.0
10
1180.7
2.6
28.0
1.7
7.1
0.0
0.2
1.7
0.0
0.2
0.0
0.0
3.5
0.0
3.7
16.8
9
1182.5
3.4
43.7
0.0
33.6
0.0
0.6
1.6
0.0
1.4
0.0
0.4
0.2
0.0
2.2
8.9
8
AC C
24
0.0
11.4
MA
9-11-37-17W4
0.0
SC
8
0.6
PT
1558.4
RI
12
1183.1
22.0
15.4
0.2
17.4
1.0
1.4
2.4
0.0
2.2
0.0
0.0
0.0
0.0
4.6
28.4
7
1183.8
1.2
69.7
0.8
14.5
0.4
0.0
1.6
0.0
0.0
0.0
0.0
0.0
0.0
1.0
5.0
6
1190.7
16.8
10.2
0.2
27.3
1.2
0.6
5.2
0.0
1.1
0.0
0.0
1.0
0.2
2.2
22.8
5
1199.8
0.0
0.0
0.0
0.0
0.0
0.0
2.6
0.0
0.0
0.0
23.7
5.4
0.0
0.0
0.0
4
1200
0.8
25.2
3.4
43.6
1.0
3.4
2.4
0.2
0.4
0.0
0.8
0.2
0.6
0.0
4.2
3
1200.5
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
2
1207.45
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
1
1207.6
0.0
3.8
2.6
0.4
0.0
0.0
1.8
0.0
0.0
0.0
0.4
4.2
0.0
0.0
1.2
0.8
30.8
0.0
55.6
0.6
0.6
3.1
0.2
0.0
0.0
0.0
0.0
0.0
2.8
4.1
12
14-29-45-23W5 25
1254
ACCEPTED MANUSCRIPT 19.1
13.9
0.0
23.3
0.0
0.2
4.0
0.0
0.4
0.0
0.0
0.0
0.0
4.6
23bis
1254.5
47.5
15.3
0.0
24.7
0.0
0.0
3.7
0.4
4.2
0.0
0.0
0.0
0.0
0.0
1.0
23
1254.75
17.8
13.1
0.0
39.9
0.0
0.4
3.1
0.0
1.4
0.0
0.0
0.0
0.0
3.5
17.2
22
1254.85
6.7
58.1
0.8
20.7
0.0
0.0
1.3
0.6
2.1
0.0
0.0
0.0
0.0
0.0
21
1255.3
0.8
43.9
1.2
3.8
0.0
0.0
10.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.6
20
1256.3
3.8
2.8
1.6
1.4
0.0
0.0
4.6
0.0
0.0
0.0
0.0
1.0
0.8
6.4
29.1
19
1257.4
0.0
5.8
0.8
0.0
0.0
0.0
0.6
0.0
0.0
0.0
0.0
0.4
0.0
0.0
18
1258.3
4.6
49.4
0.2
27.0
0.4
0.0
2.2
1.0
0.6
0.0
0.0
0.0
0.0
0.2
3.4
17
1281.4
8.6
8.6
0.0
23.3
0.0
0.6
3.3
0.0
1.0
0.0
0.0
0.0
0.0
10.3
39.1
16
1282.4
7.0
4.4
0.0
40.1
0.0
0.0
3.2
0.6
0.2
0.0
0.0
0.0
0.0
9.9
26.0
15
1282.9
3.0
18.2
0.0
26.1
0.2
0.2
0.8
0.2
0.2
0.0
0.0
0.0
0.0
7.1
41.8
14
1283.4
13.8
47.4
0.0
25.8
0.4
0.0
1.4
0.0
1.4
0.0
0.0
0.0
0.2
2.0
5.0
13
1283.7
4.3
5.7
0.0
42.6
0.0
0.0
5.3
0.0
0.8
0.0
0.0
0.0
0.0
5.9
26.8
12
1284.3
5.0
26.1
0.0
47.3
0.2
0.0
4.4
0.0
1.0
0.0
0.0
0.0
0.0
5.0
9.8
11
1285.5
6.3
5.7
0.0
35.4
0.2
0.8
3.1
0.0
1.2
0.0
0.0
0.0
0.0
12.7
29.1
10
1285.82
0.0
6.6
0.6
0.8
0.0
0.0
0.4
0.0
0.0
0.0
0.0
0.2
0.0
0.0
2.5
9
1289.6
0.0
3.0
1.0
0.2
0.0
0.0
7
1292.5
3.1
24.8
0.6
22.0
0.4
0.2
6
1321
0.0
0.2
0.4
14.3
0.0
1.2
SC
RI
PT
1254.2
29.1
3.8
0.4
0.0
0.0
0.2
0.6
0.0
0.2
2.0
10.6
0.2
0.2
0.0
1.0
0.8
0.4
3.1
15.5
7.6
0.0
0.0
0.0
0.0
1.0
0.0
2.2
29.9
NU
24
1321.35
6.9
8.1
0.0
41.0
0.6
0.6
1.6
0.2
1.4
0.2
0.0
0.0
0.0
5.7
25.6
1321.45
7.7
6.5
0.0
53.1
0.2
0.4
3.2
0.0
1.4
0.0
0.0
0.0
0.0
6.9
15.6
4
1321.5
3.8
14.9
0.2
41.0
0.2
1.0
1.6
0.2
0.6
0.0
0.0
0.2
0.0
4.8
25.9
3
1322
0.4
1.2
0.0
30.7
0.0
0.8
0.6
0.0
0.8
0.0
0.0
0.0
0.4
21.9
35.6
2
1322.5
7.1
1.0
0.0
32.3
0.4
1.3
2.5
0.2
1.7
0.0
0.0
0.0
0.4
5.4
32.1
1
1323.05
0.2
4.8
3.6
0.6
0.0
0.0
2.4
0.2
0.2
0.0
0.8
1.0
0.2
0.0
0.2
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.2
0.0
0.6
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
1323
0.0
44.0
15
1323.8
1.6
39.9
14
1325.4
0.0
2.0
13
1325.9
0.0
12
1326.1
1.0
11
1326.3
10 9 8
1327.5
0.0
12.6
7
1332.1
0.6
51.1
6
1332.3
0.4
5
1332.5
4
1335.5
3
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
23.3
0.8
0.6
3.8
0.4
0.0
0.0
0.0
0.0
0.0
4.2
25.2
21.1
34.8
0.0
19.8
0.2
0.0
1.5
0.0
3.8
0.0
0.0
0.2
0.0
2.1
13.2
1326.5
9.6
18.2
0.4
19.0
0.0
1.2
4.2
0.4
1.4
0.0
0.0
0.0
0.0
2.8
34.2
1327
10.5
22.5
0.0
22.1
0.2
0.8
5.7
0.0
1.6
0.0
0.0
0.0
0.0
2.6
17.8
0.8
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
1.2
31.5
0.8
0.2
1.6
0.0
0.2
0.0
0.0
0.2
0.0
0.2
1.8
33.7
7.8
0.6
0.0
0.0
2.6
0.0
0.0
0.0
0.0
0.6
0.0
0.2
2.0
4.2
49.2
3.1
2.2
1.6
0.2
4.7
0.0
0.9
0.0
0.5
0.7
0.9
0.0
0.7
0.6
14.5
6.7
1.8
0.0
0.0
3.8
0.0
0.0
0.0
0.0
2.4
0.0
0.6
6.3
1336.1
0.4
3.7
1.3
1.2
0.2
0.0
0.0
0.0
0.0
0.0
0.0
0.2
0.0
0.0
0.8
2
1339.8
0.0
4.2
7.0
0.0
0.0
0.0
1.0
0.0
0.0
0.0
0.0
6.0
0.0
0.0
2.8
1
1340.1
0.0
18.2
20.5
0.6
0.0
0.0
7.6
0.0
0.0
0.0
0.0
3.4
0.0
0.0
0.0
EP T
0.0
32.3
AC C
16
ED
10-36-39-22W4
MA
5 4b
06-07-40-20W4 12
1560.5
0.0
0.2
0.8
0.0
0.0
0.6
18.6
0.0
0.2
0.0
0.0
9.0
0.0
1.6
0.4
11
1561
0.0
0.0
2.2
0.0
0.0
0.8
20.8
0.0
0.8
0.0
0.0
7.0
0.0
0.0
0.4
10
1561.6
0.0
0.0
4.5
0.0
0.0
0.4
22.3
0.0
0.2
0.0
0.0
3.7
0.0
0.0
1.0
9
1562.1
0.0
0.0
4.2
0.0
0.0
0.1
4.5
0.0
0.2
0.0
0.0
4.0
0.0
0.0
0.6
8
1562.8
0.0
0.2
14.2
0.4
0.0
0.4
22.4
0.0
0.0
0.0
0.0
1.4
0.0
0.2
0.8
ACCEPTED MANUSCRIPT 7
1563.5
0.0
0.0
15.0
0.0
0.0
0.1
1.0
0.0
0.0
0.0
0.0
0.2
0.0
0.0
6
1564.1
0.0
0.0
4.4
0.0
0.0
5
1567.2
0.0
1.2
1.2
3.6
0.0
4
1564.1
0.0
0.8
1.6
0.0
3
1580.6
1.4
35.6
2.8
39.0
2
1581
0.0
2.6
0.4
1
1581.5
0.0
0.7
0.8
0.0
0.5
0.0
0.0
0.0
0.0
1.2
0.0
0.0
0.2
0.0
11.2
0.0
0.0
0.2
0.0
1.8
0.0
1.0
15.8
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.2
0.0
0.0
3.4
0.4
0.2
0.0
0.0
0.2
0.0
0.0
2.8
13.4
0.0
0.0
4.6
1.6
0.0
0.0
1.6
0.2
0.0
1.0
25.0
5.6
0.0
0.0
0.0
9.7
0.0
0.0
0.0
0.0
0.6
0.0
0.0
0.0
8-13-44-2W5 1788.85
0.0
63.5
0.0
13.7
0.0
0.2
0.6
0.0
0.0
0.0
0.0
0.6
0.0
4.6
6.8
6
1791
0.8
8.9
1.4
1.2
0.0
0.2
5.8
0.0
0.0
0.0
2.4
3.2
0.0
0.0
14.7
5
1794.6
0.0
19.7
5.1
11.3
0.0
0.8
1.4
0.0
0.0
0.0
3.4
0.2
0.0
2.2
17.4
4
1798.3
2.3
34.8
3.3
7.2
0.0
0.0
0.4
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.8
3
1798.57
4.3
15.9
0.2
56.7
0.0
0.4
2.4
0.0
1.0
2
1799.1
0.2
2.2
3.2
23.5
0.0
2.2
1.2
1
1799.97
3.0
30.0
0.0
45.5
0.0
2.0
2.2
2267.7
0.0
12.1
0.4
31.1
0.0
2.0
3
2277
0.4
9.5
0.0
40.0
0.0
0.7
2
2279
0.2
4.5
0.0
23.9
0.0
1.4
1
2289.5
0.2
30.7
0.4
22.4
0.0
918.5
0.4
20.8
5.8
12.0
4
919
1.4
31.8
6.3
3
935.2
1.9
20.7
0.6
2
935.5
0.0
2.8
2.6
1
935.9
8.1
9.9
0.2
7.1
8.2
1.4
0.0
1.8
11.9
0.2
1.0
0.0
0.0
0.0
0.0
2.6
9.9
RI
2.2
0.0
0.0
0.0
0.0
0.0
0.0
0.0
12.1
34.1
0.0
0.2
0.0
0.0
0.2
0.0
2.8
16.9
1.0
0.0
0.0
0.0
0.0
0.0
0.0
7.3
31.1
0.0
0.4
0.0
0.6
0.0
0.0
0.2
0.0
0.2
3.0
0.2
1.4
7.0
0.0
7.4
0.0
0.0
1.8
0.0
2.8
7.4
2.5
0.0
0.0
0.8
0.0
0.0
0.0
0.0
0.4
0.0
0.0
0.0
38.4
0.0
0.6
1.6
0.0
0.8
0.0
0.0
0.2
0.0
9.2
19.2
1.2
0.0
0.0
5.5
0.0
3.6
0.0
0.0
0.0
0.0
5.7
34.6
29.5
0.4
0.4
4.8
0.0
3.0
0.0
0.0
0.0
0.0
5.5
26.1
MA
ED
EP T AC C
0.0
0.0
1.2
15-08-63-05W5 5
0.0
0.4
1.0
NU
4
0.0
0.0
SC
8-4-42-5W5
PT
7
ACCEPTED MANUSCRIPT Appendix 2 Vs/Vd
SF/F
IR
V/I
T/F
W/D
S/D
TPI
GI
VI
GWI
1558.4
0.3
6.1
2.4
0.8
1.1
2.9
1.0
1.0
0.9
1.0
0.0
11
1559
0.3
8.4
3.3
0.6
0.7
4.9
1.4
1.4
0.7
1.5
0.0
10
1559.2
0.1
4.1
10.4
0.4
0.5
19.0
2.1
2.0
0.5
2.0
0.0
9
1559.6
0.4
4.9
2.3
0.4
0.6
2.4
1.3
1.4
0.4
1.3
0.9
8
1560
0.3
4.7
3.4
2.2
2.8
4.3
0.6
0.7
2.2
0.6
0.0
7
1560.5
0.4
4.5
7.1
1.9
2.2
9.7
0.9
1.0
2.0
1.0
0.0
6
1571.5
5.0
-
1.3
19.3
34.7
2.4
1.6
19.3
2.0
1.7
5
1573.9
1.2
-
4.0
10.1
12.6
15.8
1.3
2.4
10.1
2.3
11.2
4
1574.2
1.5
15.0
5.3
11.5
13.7
32.7
1.6
1.6
11.5
1.6
0.0
3
1574.6
0.4
6.2
4.4
0.7
0.9
2 1
1575 1575.8
0.1 2.1
2.9 4.5
3.0 1.3
3.0 4.1
4.0 7.4
1122.2
1.7
14.0
3.2
3.8
23
1127
0.6
3.8
5.3
3.5
22
1132.1
1.3
4.2
4.6
21
1132.45
0.8
8.5
3.2
19
1146.4
0.2
-
0.1
20
1146.8
-
-
18
1146.9
1.5
3.5
17
1149.35
1.1
12.3
16
1167.4
0.1
10.1
15
1167.8
0.2
-
14 13
1168.1 1168.6
1.2 0.2
5.7 3.8
12 11
1170 1170.5
10 9
1180.7 1182.5
8 7
1183.1 1183.8
6 5 4 3
1.5
1.4
0.8
1.5
0.1
3.1 6.5
0.4 1.8
0.4 1.9
3.2 4.3
0.4 1.8
0.0 0.1
5.0
3.0
1.3
2.2
4.1
1.3
1.1
3.8
0.8
1.0
3.5
0.8
0.7
2.6
7.7
1.8
2.0
2.2
1.9
1.3
2.2
2.9
5.8
1.1
1.2
2.2
1.1
0.7
NU
4.2
2.1
12.7
0.1
0.1
-
-
-
-
-
-
-
-
-
-
-
-
0.3
0.6
2.8
0.2
0.2
-
-
-
-
2.2
2.4
3.5
4.1
1.2
1.4
2.6
1.2
0.6
18.9
0.9
0.9
20.0
1.1
1.2
0.9
1.2
1.6
5.7
0.4
0.5
6.8
2.0
-
-
-
-
6.7 5.0
2.6 1.2
3.0 1.5
7.5 3.2
1.5 0.8
1.8 0.9
2.7 1.3
1.5 0.8
0.6 0.8
MA
1.4
-
ED
EP T
6.1
2.8
-
20.0
20.6
21.6
165.5
2.9
3.8
20.6
3.6
0.3
3.5 1.4
4.5 4.0
0.9 3.5
0.9 5.6
1.9 7.3
2.3 11.2
1.7 1.5
1.8 1.6
1.0 5.7
1.6 1.5
0.5 0.4
2.1 4.6
6.2 5.0
7.5 2.5
1.5 10.3
1.7 14.4
11.4 20.2
3.0 4.0
3.3 4.6
1.6 10.6
3.1 4.2
0.4 0.2
1.0
10.4
2.6
1.6
2.3
3.9
1.3
1.4
1.7
1.3
0.6
1199.8
-
-
-
-
-
-
-
-
-
-
-
1200
0.6
-
5.3
15.5
18.4
7.9
0.6
0.7
16.1
0.6
0.9
AC C
24
18.7
SC
9-11-37-17W4
PT
12
RI
Well/ Depth sample (m) 10-25-40-25W4
1190.7
1200.5
-
-
-
-
-
-
-
-
-
-
-
2
1207.45
-
-
-
-
-
-
-
-
-
-
-
1
1207.6
1.3
-
-
5.7
5.7
2.3
1.0
-
-
-
-
10.9
12.8
9.0
0.6
0.7
10.9
0.6
0.0
14-29-45-23W5 25
1254
0.6
1.5
5.8
24
1254.2
1.4
6.3
13.0
1.6
1.7
10.1
2.2
2.6
1.6
2.2
0.1
23bis
1254.5
2.5
-
0.8
39.8
87.5
17.2
2.2
2.6
87.5
2.4
0.0
23
1254.75
0.8
4.9
9.4
3.1
3.4
10.1
1.1
1.2
-
1.2
-
22
1254.85
3.0
-
-
-
-
49.8
2.8
3.1
-
3.0
0.1
21
1255.3
8.9
-
-
82.8
82.8
4.5
3.0
11.9
82.8
3.3
0.8
1256.3
2.2
1.4
1.5
1.3
1.4
2.9
19
1257.4
7.3
-
-
-
18
1258.3
2.0
17.0
9.0
20.4
-
9.7
4.1
22.7
24.0
1.9
-
-
5.8
15.9
2.1
21.5
1.9
0.1
17
1281.4
0.7
3.8
11.8
0.8
0.8
9.4
2.2
2.4
0.8
2.2
0.0
16
1282.4
0.3
2.6
4.3
1.2
15
1282.9
0.8
5.9
22.2
0.9
1.4
4.2
1.0
25.0
0.9
1.0
1.2
0.9
0.0
2.4
2.5
0.9
2.4
0.0
14
1283.4
2.4
2.5
11.7
11.5
12.5
34.1
2.5
2.6
11.5
2.5
0.0
13
1283.7
0.2
4.5
12
1284.3
0.7
2.0
4.0
1.3
12.3
4.9
1.6
3.2
0.8
0.8
1.3
0.8
0.0
5.3
8.2
0.9
0.9
4.9
0.9
0.0
11
1285.5
0.3
2.3
10
1285.82
4.7
-
7.6
1.0
-
3.2
1.2
6.3
1.2
1.3
1.0
1.3
0.0
3.2
22.8
5.1
11.4
3.2
6.5
12.0
9
1289.6
2.5
10.0
2.2
1.3
1.9
1.0
0.8
4.3
1.3
0.8
27.4
7
1292.5
6
1321
1.2
5.0
0.0
13.6
2.5
2.0
2.7
2.6
1.1
1.6
2.1
1.1
0.2
0.7
0.2
0.5
0.7
0.5
0.6
0.2
0.5
0.1
5
1321.35
0.4
4.5
4.1
1.5
1.8
5.4
0.9
1.0
1.5
1.0
0.0
4b
1321.45
4
1321.5
0.3
2.3
4.5
2.5
3.0
0.5
5.4
5.5
1.7
3
1322
0.1
1.6
7.8
0.5
2
1322.5
0.3
5.9
2.5
1
1323.05
1.2
-
1.0
-
10-36-39-22W4
0.2
0.3
1.6
4.5
0.6
2.5
0.6
0.0
2.0
9.9
0.6 1.1
1.1
1.8
1.1
0.0
0.6
13.1
1.7
1.6
0.6
1.7
0.0
0.8
1.1
3.4
1.0
1.0
0.9
1.0
0.1
23.0
46.0
1.5
0.7
6.5
23.0
1.0
15.3
NU
4.5
SC
20
RI
0.2
PT
ACCEPTED MANUSCRIPT
1323
-
-
15
1323.8
-
-
14
1325.4
-
-
13
1325.9
-
-
-
-
-
-
-
-
-
-
-
12
1326.1
1.4
6.0
4.1
1.6
2.0
7.4
2.0
2.1
1.7
1.9
0.0
11
1326.3
2.8
6.3
38.3
4.8
5.0
47.5
3.3
3.5
5.0
3.5
0.0
10
1326.5
1.4
12.2
61.7
1.3
1.3
15.4
2.7
3.3
1.3
2.8
0.2
9
1327
1.5
6.8
1.3
1.5
2.8
2.6
1.2
1.4
1.6
1.3
0.0
8
1327.5
7
1332.1
6
1332.3
5
1332.5
4
1335.5
2 1
-
-
-
-
-
-
-
-
-
-
-
-
-
-
-
-
-
-
-
-
-
-
-
-
ED
EP T -
-
-
-
-
-
-
-
-
-
-
1.6
9.0
-
42.7
42.7
33.6
1.6
1.7
42.7
1.6
0.1
4.1
10.0
11.0
17.7
19.3
13.0
3.2
45.4
17.7
9.1
1.5
10.1
-
3.5
67.2
86.4
11.5
5.2
22.5
86.4
6.8
0.6
1.8
10.5
2.0
2.3
3.4
3.1
1.4
4.2
2.3
2.0
3.5
1336.1
1.6
-
4.0
6.8
8.5
24.5
1.8
3.5
6.8
3.1
17.4
1339.8
0.6
-
14.0
3.7
4.0
5.8
0.9
35.0
3.7
1.0
18.8
1340.1
0.9
-
0.0
13.1
-
1.7
0.6
5.1
13.1
1.2
2.5
AC C
3
-
-
MA
16
06-07-40-20W4 12
1560.5
0.3
0.3
0.0
0.0
0.8
0.1
0.0
0.0
0.0
0.0
72.0
11
1561
0.0
-
0.0
0.0
7.5
0.0
0.0
0.0
0.0
0.0
-
10
1561.6
0.0
-
0.0
0.1
5.0
0.1
0.0
0.0
0.1
0.0
-
9
1562.1
0.0
-
0.0
0.1
7.7
0.1
0.0
0.0
0.1
0.0
-
8
1562.8
0.0
4.0
0.1
0.8
14.8
0.8
0.0
0.1
0.8
0.1
312.0
7
1563.5
0.0
-
0.1
1.2
18.8
1.3
0.0
0.1
1.2
0.1
-
6
1564.1
0.0
-
0.1
1.3
22.0
1.4
0.0
0.1
1.3
0.0
-
5
1567.2
0.3
15.8
0.3
0.1
0.4
0.4
0.3
0.3
0.1
0.3
16.2
4
1564.1
0.5
-
-
12.0
12.0
-
0.6
-
12.0
-
121.8
3
1580.6
0.9
-
3.5
21.9
28.1
37.2
0.9
1.0
23.2
0.9
1.4
ACCEPTED MANUSCRIPT 2
1581
0.2
25.0
1.0
0.3
0.6
1.8
0.7
0.7
0.4
0.7
14.6
1
1581.5
0.1
-
0.0
0.8
-
0.7
0.0
0.1
0.8
0.0
108.4
4.6
1.5
1.5
4.1
6.8
12.9
3.8
3.5
4.8
3.7
0.0
6
1791
3.7
-
14.7
0.8
0.9
2.7
2.1
11.1
0.8
1.8
5.6
5
1794.6
1.2
7.9
6.5
1.6
1.9
6.0
1.7
2.7
1.8
2.2
1.2
4
1798.3
3.5
-
0.1
7.7
59.5
6.5
2.3
3.0
7.7
2.9
1.0
3
1798.57
0.4
1.2
25.5
4.9
5.1
11.8
0.6
0.6
4.9
0.6
0.0
2
1799.1
0.1
6.6
0.3
0.6
2.3
0.4
0.2
0.3
0.6
0.3
0.6
1
1799.97
0.7
3.8
4.2
5.2
6.4
9.5
0.9
0.9
5.4
0.9
0.0
1.5
0.9
1.5
0.1
0.6
0.6
2.0
0.6
0.4
PT
1788.85
1.5
1.7
0.9
0.9
0.5
0.9
0.2
21.3
1.4
1.4
12.3
1.4
0.8
SC
7
RI
8-13-44-2W5
8-4-42-5W5 4
2267.7
0.4
2.8
6.8
0.9
1.0
8.1
3
2277
0.2
6.0
2.4
1.8
2.6
3.7
2
2279
0.2
4.3
1.5
0.5
0.8
1
2289.5
1.4
15.0
2.3
11.7
16.8
15-08-63-05W5 5
918.5
1.2
2.6
0.5
1.3
4
919
3.8
-
-
-
3
935.2
0.6
2.1
4.2
1.8
2
935.5
0.7
6.1
1.2
1
935.9
0.6
4.7
2.7
1.2
0.7
1.0
1.4
1.0
0.4
-
42.3
3.4
13.0
-
8.9
1.6
6.5
1.1
1.1
1.8
1.1
0.0
0.2
1.1
1.0
1.2
0.1
1.2
2.5
1.1
1.5
3.4
1.1
1.2
1.2
1.2
0.0
NU
2.2
0.1
MA ED EP T AC C
4.0
ACCEPTED MANUSCRIPT
Depth (m)
M oist (%)
Ash (%)
Volatil M atter (%)
C (%)
H (%)
N (%)
S (%)
12
1558.4
3.13
1.71
29.13
83.38
4.64
1.34
0.42
11
1559
3.14
2.35
29.24
79.18
4.47
1.27
0.38
10
1559.2
2.04
67.82
11.59
21.43
1.71
0.45
0.27
9
1559.6
2.36
32.66
20.32
52.85
3.28
0.75
0.28
8
1560
2.99
4.28
34.20
78.36
5.01
1.66
0.65
7
1560.5
2.36
13.49
36.23
68.17
4.25
1.17
6
1571.5
2.29
58.16
19.24
28.96
2.48
0.69
4.18
5
1573.9
2.13
39.11
29.76
45.93
3.36
0.98
9.36
4
1574.2
2.85
7.85
37.48
73.97
PT
0.45
5.04
1.60
0.54
3
1574.6
2.73
8.31
31.27
76.34
4.67
1.36
1.52
2
1575
2.73
33.47
28.08
51.75
RI
Appendi x 3 – Elemental Analysis data Well/sample
3.89
1.08
1.20
1
1575.8
1.25
89.08
5.86
6.66
0.88
0.25
0.11
24
1122.2
4.45
50.15
20.57
35.95
2.57
0.80
0.58
23
1127
5.14
2.46
44.29
75.14
2.30
1.50
0.72
22
1132.1
3.91
42.17
20.36
33.42
2.43
0.88
0.70
21
1132.45
5.40
3.69
33.80
74.55
4.23
1.56
0.52
19
1146.4
3.72
59.98
16.96
25.91
2.11
0.68
0.29
20
1146.8
2.93
81.04
11.03
10.27
1.25
0.45
0.49
18
1146.9
3.12
73.20
15.06
14.47
1.75
0.42
0.25
17
1149.35
4.19
15.48
16
1167.4
3.84
15
1167.8
2.07
14
1168.1
4.62
13
1168.6
5.19
12
1170
2.53
11
1170.5
6.18
10
1180.7
4.72
9
1182.5
8
1183.1
59.77
3.59
1.22
9.70
22.74
37.97
2.68
0.89
1.95
56.41
33.97
26.08
1.50
0.50
0.34
25.64
29.97
54.59
3.65
1.21
1.13
2.81
36.01
75.60
4.54
1.53
0.57
86.69
8.28
6.33
0.97
0.34
0.86
10.48
32.29
67.44
4.25
1.48
0.49
33.32
22.97
50.37
3.04
0.95
0.42
5.82
1.76
38.06
75.15
4.94
1.38
0.77
5.14
3.36
37.28
74.08
4.76
1.50
0.75
1183.8
5.99
6.05
37.24
70.93
4.69
1.49
1.68
1190.7
5.38
3.86
33.44
75.58
4.37
1.33
0.45
1199.8
4.5
92.46
6.8
2.7
0.73
0.23
0.07
1200
5.12
26.92
31.9
52.36
3.78
1.15
3.56
3
1200.5
6.47
90.05
6.66
3.08
0.78
0.24
0.57
2 1
1207.45 1207.6
3.96 3.59
84.86 83.01
10.62 9.46
5.38 8.92
1.14 1.02
0.24 0.37
0.24 0.6
25
1254
2.97
7.42
39.34
72.37
5.05
1.41
5.53
7 6 5 4
EP T
ED
31.99
45.82
AC C
MA
NU
9-11-37-17W4
SC
10-25-40-25W4
14-29-45-23W5 24
1254.2
3.41
2.56
37.73
78.45
5.12
1.84
1.23
23bis
1254.5
2.64
16.83
27.41
68.94
4.07
1.24
2.03
23
1254.75
2.88
12.59
34.79
69.71
4.67
1.49
0.92
22
1254.85
3.25
16.07
35.95
62.86
4.35
1.44
8.55
21
1255.3
2.35
59.99
18.61
25.28
2.28
0.67
6.04
4.14
1.19
1.87
7.66
5.26
1.03
0.27
0.28
36.63
68.43
4.80
1.50
2.50
27.93
48.93
3.07
0.75
16.81
2.85
37.23
78.77
5.01
1.50
0.99
2.35
34.82
79.42
4.92
1.68
0.70
3.20
11.72
32.28
71.86
4.41
1.46
0.71
1283.7
2.81
4.78
35.76
77.96
4.94
1.44
0.65
1284.3
3.07
1.12
33.64
80.98
4.78
1.52
0.65
11
1285.5
2.95
1.46
37.75
80.64
5.07
1.74
0.75
10
1285.82
1.80
90.17
7.45
2.92
0.90
0.12
9
1289.6
2.30
86.77
8.20
6.37
1.09
0.16
0.08
7
1292.5
3.12
19.43
28.75
67.66
4.29
1.16
0.68
6
1321
3.00
4.98
26.01
80.38
PT
0.72
4.13
1.11
0.27
5
1321.35
3.71
2.07
2.07
81.65
4.99
1.47
0.44
4b
1321.45
3.02
2.73
2.73
80.19
RI
1256.3
3.13
21.14
19
1257.4
1.66
88.45
18
1258.3
2.82
13.93
17
1281.4
1.80
27.09
16
1282.4
3.00
15
1282.9
3.46
14
1283.4
13 12
4.99
1.45
0.55
4
1321.5
3.20
2.06
2.06
80.44
4.69
1.25
0.77
3
1322
3.21
4.84
4.84
79.69
4.68
1.31
0.33
2
1322.5
2.62
7.64
7.64
76.65
4.36
1.23
0.39
1
1323.05
3.13
88.47
7.44
5.55
0.99
0.18
0.34
16
1323
1.96
86.07
7.17
7.47
1.06
0.32
0.20
15
1323.8
2.23
83.69
8.45
8.98
1.13
0.33
0.83
14
1325.4
2.17
92.07
6.30
2.33
0.84
0.22
0.12
13
1325.9
5.10
5.97
35.65
72.79
4.63
1.46
2.62
12
1326.1
3.46
9.71
28.24
73.43
3.92
1.19
3.63
11
1326.3
4.55
2.05
35.51
79.86
5.04
1.48
0.50
10
1326.5
4.26
1.49
34.73
80.68
4.93
1.52
0.50
9
1327
3.65
1.92
34.74
80.39
4.95
1.49
0.49
8
1327.5
1.62
93.04
6.11
1.44
0.83
0.19
0.09
7
1332.1
3.92
14.62
33.49
67.67
4.53
1.57
0.93
6
1332.3
3.59
49.48
25.29
36.95
2.98
0.92
2.06
5
1332.5
3.93
20.97
29.53
59.24
3.99
1.20
4.14
4
1335.5
3.29
67.83
14.42
22.50
2.02
0.56
0.34
1336.1
3.08
89.83
7.45
3.45
0.98
0.25
0.84
1339.8
3.10
86.43
9.25
5.95
1.17
0.26
0.27
1340.1
2.89
65.97
16.47
22.61
2.08
0.63
2.32
12
1560.5
2.13
44.46
18.23
43.77
2.85
0.62
0.30
11
1561
1.88
50.14
19.10
47.94
2.98
0.71
0.32
10
1561.6
2.34
37.46
19.23
50.04
3.05
0.83
0.36
9
1562.1
2.69
35.69
20.27
51.28
3.13
0.84
0.36
8
1562.8
1.98
71.62
11.18
19.73
1.71
0.51
0.23
7
1563.5
1.87
77.41
9.91
14.74
1.43
0.43
0.21
6
1564.1
1.41
89.78
6.82
4.49
0.81
0.23
0.08
5
1567.2
2.46
29.56
22.53
56.93
3.50
1.05
0.41
4
1564.1
1.76
93.54
5.00
1.71
0.68
0.16
0.10
3
1580.6
2.47
5.44
39.41
77.24
5.32
1.71
1.42
3 2 1
EP T
ED
MA
10-36-39-22W4
27.67
NU
20
SC
63.63
AC C
ACCEPTED MANUSCRIPT
06-07-40-20W4
2
1581
2.70
37.29
17.48
50.50
2.90
0.67
0.35
1
1581.5
2.41
84.38
8.64
8.96
1.09
0.25
1.00
7
1788.85
2.12
13.13
29.85
66.15
4.07
1.03
7.52
6
1791
1.84
52.45
20.96
35.20
2.76
0.68
4.71
5
1794.6
1.61
35.13
26.34
51.83
3.68
0.89
3.76
4
1798.3
1.52
31.43
29.68
44.12
3.17
0.67
16.66
3
1798.57
1.73
8.24
34.87
76.80
5.10
1.39
1.27
2
1799.1
1.05
37.63
21.30
52.47
3.29
0.72
0.76
1
1799.97
1.70
4.97
34.97
79.80
5.02
1.47
1.14
4
2267.7
1.10
7.22
31.25
79.99
4.78
1.14
2277
0.99
13.00
27.26
75.58
PT
1.86
3
4.44
1.08
0.97
2
2279
0.94
56.98
16.52
30.85
1.96
0.51
9.43
1
2289.5
0.90
36.18
26.42
51.75
RI
ACCEPTED MANUSCRIPT
3.69
1.00
1.95
5
918.5
3.37
31.70
23.65
55.75
3.36
1.05
0.51
4
919
3.01
71.83
13.76
18.23
1.69
0.52
1.78
3
935.2
3.54
21.19
26.29
63.69
3.78
1.21
0.32
2
935.5
3.67
29.49
21.94
73.09
4.59
1.50
0.39
1
935.9
3.96
5.80
32.15
78.64
4.71
1.42
0.35
8-13-44-2W5
ED
MA
NU
15-08-63-05W5
SC
8-4-42-5W5
EP T
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Hayes, B., J. Christopher, L. Rosenthal, G. Los, B. McKercher, D. Minken, Y. Tremblay, J. Fennell, and D. Smith, 1994, Cretaceous Mannville Group of the western Canada
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sedimentary basin, Geological Atlas of the Western Canada sedimentary basin, v. 4, Canadian Society of Petroleum Geologists and Alberta Research Council, p. 317-334.
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Holz, M., W. Kalkreuth, and I. Banerjee, 2002, Sequence stratigraphy of paralic coal-bearing strata: an overview: International Journal of Coal Geology, v. 48, p. 147-179. ICCP, 1998, The new vitrinite classification (ICCP System 1994): Fuel, v. 77, p. 349-358.
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ICCP, 2001, The new inertinite classification (ICCP System 1994): Fuel, v. 80, p. 459-471. ISO-562, 1998, Hard coal and coke - Determination of volatile matter. ISO-7404-2, 2009, Methods for the Petrographic Analysis of Coals — Part 2: Methods of Preparing Coal Samples, International Organization for Standardization Geneva, Switzerland, p. 12 pp. Jackson, P. C., 1984, Paleogeography of the Lower Cretaceous Mannville group of western Canada.
ACCEPTED MANUSCRIPT Kalkreuth, W., and D. A. Leckie, 1989, Sedimentological and petrographical characteristics of Cretaceous strandplain coals: a model for coal accumulation from the North American Western Interior Seaway: International Journal of Coal Geology, v. 12, p. 381-424. Kalkreuth, W., D. Marchioni, J. Calder, M. Lamberson, R. Naylor, and J. Paul, 1991, The relationship between coal petrography and depositional environments from selected
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coal basins in Canada: International Journal of Coal Geology, v. 19, p. 21-76. Lafargue, E., F. Marquis, and D. Pillot, 1998, Rock-Eval 6 applications in hydrocarbon
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exploration, production, and soil contamination studies: Oil & Gas Science and
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Technology, v. 53, p. 421-437.
Lamberson, M., R. Bustin, and W. Kalkreuth, 1991, Lithotype (maceral) composition and
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variation as correlated with paleo-wetland environments, Gates Formation, northeastern British Columbia, Canada: International Journal of Coal Geology, v. 18, p. 87-124.
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Langenberg, C., B. Rottenfusser, and R. Richardson, 1997, Coal and coalbed methane in the Mannville Group and its equivalents, Alberta. In: Pemberton, S.G. and James, D.P.
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(eds.). Petroleum Geology of the Cretaceous Mannville Group, Western Canada.: Canadian Society of Petroleum Geologists, v. Memoir 18, p. 475-486.
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Marchioni, D., and W. Kalkreuth, 1991, Coal facies interpretations based on lithotype and maceral variations in Lower Cretaceous (Gates Formation) coals of Western Canada: International Journal of Coal Geology, v. 18, p. 125-162.
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Moore, T., and J. Shearer, 2003, Peat/coal type and depositional environment—are they related?: International Journal of Coal Geology, v. 56, p. 233-252. Nicolas, G., B. Pradier, and F. Vannier-Petit, 1997, Reconstitution des environnements de dépôt des sédiments organiques de plaine deltaıque. Application al’étude sédimentologique du groupe Brent (Mer du Nord): Bulletin du Centre de Recherches Elf Exploration Production, v. 21, p. 249-264. Peters, K., 1986, Guidelines for evaluating petroleum source rock using programmed pyrolysis: AAPG bulletin, v. 70, p. 318-329.
ACCEPTED MANUSCRIPT Petersen, H., 1993, Petrographic facies analysis of Lower and Middle Jurassic coal seams on the island of Bornholm, Denmark: International Journal of Coal Geology, v. 22, p. 189-216. Pickel, W., Kus, J., Flores, D., Kalaitzidis, S., Christanis, K., Cardott, B., Misz-Kennan, M., Rodrigues, S., Hentschel, A. and Hamor-Vido, M., 2017. Classification of liptinite– ICCP System 1994. International Journal of Coal Geology, 169: 40-61.
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Stach, E., M.-T. Mackowsky, M. Teichmüller, G. Taylor, D. Chandra, and R. Teichmüller, 1982, Coal petrology: Gebrüder Borntraeger, Berlin, p. 535.
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Staub, J. R., 2002, Marine flooding events and coal bed sequence architecture in southern West
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Virginia: International Journal of Coal Geology, v. 49, p. 123-145. Strobl, R., 1988, The effects of sea-level fluctuations on prograding shoreline sand estuarine
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valley fill sequences in the Glauconitic member, Medicine River field and adjacent areas. In: D.P. James and D.A. Leckie (eds.). Sequences, Sedimentology: Surface and
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Subsurface. : Canadian Society of Petroleum Geologists, v. Memoir 15, p. 221-236. Styan, W. t., and R. Bustin, 1983, Petrographyof some fraser river delta peat deposits: coal
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maceral and microlithotype precursors in temperate-climate peats: International Journal of Coal Geology, v. 2, p. 321-370.
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Suárez-Ruiz, I., D. Flores, J. G. Mendonça Filho, and P. C. Hackley, 2012, Review and update of the applications of organic petrology: Part 1, geological applications: International Journal of Coal Geology, v. 99, p. 54-112.
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Sýkorová, I., W. Pickel, K. Christanis, M. Wolf, G. Taylor, and D. Flores, 2005, Classification of huminite—ICCP System 1994: International Journal of Coal Geology, v. 62, p. 85106.
Teichmüller, M. and Teichmüller, R., 1982. Fundamentals of coal petrology. Stach, E., Mackowsky, M.-Th., Teichmüller, M., Taylor, GH, Chandra, D., and Techmüller, R., Stach’s Textbook of Coal Petrology, 3rd revised and enlarged edition: Berlin, Stuttgart, Gebrüder Borntraeger: 5-86. Teichmüller, M., 1989, The genesis of coal from the viewpoint of coal petrology: International Journal of Coal Geology, v. 12, p. 1-87.
ACCEPTED MANUSCRIPT Tyson, R., 2001, Sedimentation rate, dilution, preservation and total organic carbon: some results of a modelling study: Organic Geochemistry, v. 32, p. 333-339. Wadsworth, J., R. Boyd, C. Diessel, D. Leckie, and B. A. Zaitlin, 2002, Stratigraphic style of coal and non-marine strata in a tectonically influenced intermediate accommodation setting: the Mannville Group of the Western Canadian Sedimentary Basin, south-central
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Alberta: Bulletin of Canadian Petroleum Geology, v. 50, p. 507-541. Wadsworth, J., R. Boyd, C. Diessel, and D. Leckie, 2003, Stratigraphic style of coal and non-
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marine strata in a high accommodation setting: Falher Member and Gates Formation
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(Lower Cretaceous), western Canada: Bulletin of Canadian Petroleum Geology, v. 51, p. 275-303.
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Wadsworth, J., C. Diessel, and R. Boyd, 2010, The sequence-stratigraphic significance of paralic coal and its use as an indicator of accommodation space in terrestrial sediments:
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Application of modern stratigraphic techniques: Theory and case histories: SEPM
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Special Publication, v. 94, p. 201-221.
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Figures
Fig. 1 – Location of the study area and distribution of the Mannville Group deposits. The paleogeography
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at the end of the deposition of the Upper Mannville Group and the lithology distribution is indicated (Jackson 1984). The trace line of the geological transect of Fig. 2 is shown together with the location of
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the well-logs and cores analyzed in this work.
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Fig. 2 – Geological section showing the architecture and geometry of the Mannville Group (From Deschamps et al., in press). The stratigraphic record has been subdivided in the 3rd -order system tracts. The position of the core analyzed in this work is also indicated. The trace line of the section is shown in Fig. 1.
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Fig. 3 (Part a)
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Fig. 3 (Part b) Fig. 3 – Stratigraphic section of the cores analyzed. The stratigraphic record was subdivided in 4 th -order depositional sequences. In correspondence of the coal packages 5th -order deepening and shallowing cycles were also recognized. For each sample the depositional environment where coal formed is defined,
ACCEPTED MANUSCRIPT by means of interpretation of the TPI and GI indices (Fig. 4). Location of the cores is shown in Fig. 2 and
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1.
Fig. 4 - GI-TPI facies diagram proposed by Diessel (1986) and modified by Nicolas et al., (1997), which determines the depositional environment of the peat.
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Fig. 5 – Block-diagram illustrating the spatial distribution of the coal depositional environments
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throughout the alluvial and delta plain (Modified from Nicolas et al., 1997). Variation in the subsidence rate along the sedimentary profile determine a different vertical superimposition of the depositional
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environments.
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Fig. 6 – Optical microscopy, photomicrographs taken under reflected white light. Fluorescence mode in photographs (b) and (f). Width of the longitudinal dimension of the pictures: 200 μm. Terrestrial depositional environments (a-d): (a and c) Organic matter accumulation formed by very small fragments of inertinite macerals (inertodetrinite) spore and mineral matter. Sporinite is visible in fluorescence mode (b); (d) Collodetrinite binding mostly fusinite, semifusinite macerals and mineral matter. Dry Forest depositional environment (e-h): (e) Fusinite, semifusinite and liptinite. Liptinite in fluorescence mode (f) appears as exsudatinite; (g) Fusinite and semifusinite macerals; (h) Collodetrinite binding semifusinite maceral and liptinite, where cell lumens are still recognizable.
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Fig. 7 - Optical microscopy, photomicrographs taken under reflected white light. Fluorescence mode in photographs (d) and (h). Width of the longitudinal dimension of the pictures: 200 μm. Wet Forest depositional environment (a-e): Collotellinite on the top of the photogram and telinite on the bottom. In telinite cell lumens are filled with resinite; (b) Collotellinite where cell walls are not completely homogenized; (c) Collodetrinite binding fusinite, semifusinite and sporinite macerals. On the bottom right of the image a big spore is visible in fluorescence mode (d). Swamp Forest (e-h): (e) interstratified layers of vitrinite, sporinite, resinite and mineral matter. On the top right of the image large accumulation of pyrite can be observed; (f) Fusinite with cell lumens filled with mineral matter; (g) Collodetrinite binding, vitrodetrinite, cutinite, sporinite and mineral matter. Cutinite ,sporinite and exsudatinite can be observed in fluorescence mode (h).
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Fig. 8 - Optical microscopy, photomicrographs taken under reflected white light. Fluorescence mode in photographs (d) and (h). Width of the longitudinal dimension of the pictures: 200 μm. Reed Moor depositional environment (a-d): (a and c) Collodetrinite and sporinite, inertodetrinite, semifusinite and mineral matter. Sporinite is visible in fluorescence mode (d); (b) Collodetrinite binding sporinite, inertodetrinite and funginite. Limnic depositional environment (e-h): (e) Organic matter accumulation formed by vitrinite (collotellinite and vitrodetrinite), semifusinite and sporinite, interstratified with mineral matter; (f) Collodetrinite
ACCEPTED MANUSCRIPT binding sporinite of different size and semifusinite; (g) Vitrinite layers interstratified with sporinite,
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semifusinite and algae; (h) In fluorescence mode, algae are well recognizable as Botryococcus braunii.
Fig. 9 - Optical microscopy, photomicrographs taken under reflected white light. Fluorescence mode in photographs (b) and (h). Width of the longitudinal dimension of the pictures : 200 μm.
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Open Moor depositional environments, formed by organic matter dispersed in mineral matter (DOM): (a, c and d) Layers of organic matter, formed by vitrinite, semifusinite, inertodetrinite and sporinite, interstratified with mineral matter. Sporinite is visible in fluorescence mode (b); (e, f and g) Fragments of organic matter, with different composition, size and preservation state, transported and deposited together with abundant mineral matter. Sporinite can be also accumulated in these deposits (h); In (e) on the right, large accumulation of pyrite and in (f) carbonate clasts deposited with organic matter fragments.
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Fig. 10 - Frequency of the occurrence of the coal depositional environments in the 4th-order system
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tracts.
ACCEPTED MANUSCRIPT
S ample
Depht
Lithofacies
10-25-40-25W4
12
1558.4
Coal
HST
HST
Sh
Terrestrial / Dry Forest
11
1559
Coal
HST
HST
Sh
Terrestrial
10
1559.2
Coal
HST
HST
Sh
Terrestrial
9
1559.6
Coal
HST
HST
Sh
Terrestrial
8
1560
Coal
HST
HST
Sh
Reed M oor
7
1560.5
Coal
HST
HST
Sh
Reed M oor
6
1571.5
DOM
TST
TST
Dp
5
1573.9
DOM
TST
TST
Dp
4
1574.2
Coal
TST
TST
3
1574.6
Coal
TST
TST
2
1575
Coal
TST
1
1575.8
Coal
TST
23
1127
Coal
22
1132.1
Coal
21
1132.45
Coal
20
1144.8
Coal
19
1146.4
18 17
5th
Depositional Environment
Open M oor
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Open M oor
Sh
Terrestrial
TST
Sh
Reed M oor
TST
Sh
Wet Forest / Swamp Forest
HST
TST
Sh
Liminic / Reed M oor
HST
HST
Sh
Dry Forest
HST
M FS
M FS
Reed M oor
HST
M FS
M FS
Open M oor
DOM
HST
TST
Dp
Open M oor
1146.9
DOM
HST
TST
Dp
Open M oor
1149.35
Coal
HST
TST
Sh
Reed M oor
1167.4
Coal
HST
HST
Sh
Terrestrial / Dry Forest
1167.8
DOM
HST
HST
Sh
Open M oor
1168.1
Coal
HST
HST
Dp
Dry Forest / Wet Forest
13
1168.6
Coal
HST
HST
Sh
Dry Forest
12
1170
DOM
HST
M FS
M FS
Open M oor
11
1170.5
Coal
HST
TST
Dp
Swamp Forest
10
1180.7
Coal
TST
HST
Sh
Dry Forest / Terrestrial
9
1182.5
Coal
TST
HST
Sh
Swamp Forest / Limnic
8
1183.1
Coal
TST
HST
Sh
Dry Forest
7
1183.8
Coal
TST
TST
Dp
Wet Forest / Swamp Forest
6
1190.7
Coal
LST
HST
Sh
Dry Forest / Reed M oor
5
1199.8
DOM
LST
TST
M FS
Open M oor
4
1200
DOM
LST
TST
Sh
Limnic
16 15
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14
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Swamp Forest / Limnic
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4th
Dp
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9-11-37-17W4
3rd
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Well
ACCEPTED MANUSCRIPT 1200.5
Shale
LST
TST
M FS
Open M oor
2
1207.45
Shale
LST
TST
Dp
Open M oor
1
1207.6
DOM
LST
TST
Dp
Open M oor
24
1122.2
Coal
HST
M FS
M FS
Wet Forest / Swamp Forest
Coal
HST
HST
Sh
Limnic
25
1254 1254.2
Coal
HST
HST
Sh
Dry Forest
23bis
1254.5
Coal
HST
HST
Sh
Swamp Forest
23
1254.75
Coal
HST
HST
Sh
22
1254.85
Coal
HST
HST
Sh
21
1255.3
Coal
HST
HST
20
1256.3
Coal
HST
HST
19
1257.4
DOM
HST
18
1258.3
Coal
HST
17
1281.4
Coal
HST
16
1282.4
Coal
HST
15
1282.9
Coal
14
1283.4
Coal
13
1283.7
Coal
12
1284.3
11
1285.5
10
? Reed M oor, Dry forest
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? Limnic, Swamp, Wet Forest Wet Forest
Sh
Terrestrial
SC
Sh
M FS
Open M oor
HST
Sh
Swamp Forest
HST
Sh
Dry Forest
HST
Sh
Dry Forest / Reed M oor
HST
HST
Sh
Dry Forest
HST
HST
Sh
Swamp Forest
HST
HST
M FS
Dry Forest / Reed M oor
Coal
HST
HST
Dp
Limnic
Coal
HST
HST
Sh
Dry Forest
ED
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HST
1285.82
DOM
HST
HST
Sh
Open M oor
1289.6
DOM
HST
HST
Sh
Open M oor
1292.5
Coal
HST
HST
Sh
Dry Forest / Reed M oor
1321
Coal
HST
HST
Sh
Terrestrial
5
1321.35
Coal
HST
HST
Sh
Dry Forest / Reed M oor
4b
1321.45
Coal
HST
HST
Sh
Reed M oor
4
1321.5
Coal
HST
HST
Sh
Dry Forest / Reed M oor
3
1322
Coal
HST
HST
Sh
Terrestrial
2
1322.5
Coal
HST
HST
Sh
Dry Forest
1
1323
DOM
HST
M FS
M FS
Open M oor
16
1323
DOM
HST
HST
Sh
Open M oor
15
1323.8
DOM
HST
HST
Sh
Open M oor
14
1325.4
DOM
HST
M FS
Sh
Open M oor
9 7
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6
10-36-39-22W4
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24
EP T
14-29-45-23W5
3
ACCEPTED MANUSCRIPT 13
1325.9
DOM -
HST
TST
Dp
Open M oor
Pyrite Coal
HST
TST
Sh
Dry Forest
11
1326.3
Coal
HST
TST
Sh
Wet Forest
10
1326.5
Coal
HST
TST
Sh
Dry Forest
9
1327
Coal
HST
TST
Sh
Dry Forest
8
1327.5
DOM
HST
TST
M FS
Open M oor
7
1332.1
Coal
TST
TST
Sh
Swamp Forest
6
1332.3
DOM
TST
TST
Sh
5
1332.5
DOM
TST
TST
M FS
Open M oor
4
1335.5
DOM
TST
TST
Sh
Open M oor
3
1336.1
DOM
TST
2
1339.8
DOM
TST
1
1340.1
DOM
TST
12
1560.5
Coal
HST
11
1561
Coal
10
1561.6
Coal
9
1562.1
Coal
8
1562.8
7
1563.5
6
M FS
Open M oor
HST
Sh
Open M oor
HST
M FS
Open M oor
HST
Sh
Terrestrial
HST
HST
Sh
Terrestrial
HST
HST
Sh
Terrestrial
HST
HST
Sh
Terrestrial
DOM
HST
HST
Sh
Open M oor
DOM
HST
HST
Sh
Open M oor
ED
MA
TST
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SC
RI
Open M oor
1564.1
DOM
HST
HST
Sh
Open M oor
1567.2
Coal
HST
TST
Sh
Terrestrial
1567.5
DOM
HST
TST
M FS
Open M oor
1580.6
Coal
TST
HST
Sh
Limnic
2
1581
Coal
TST
HST
Sh
Terrestrial
1
1581.5
DOM
TST
M FS
M FS
Open M oor
7
1788.85
Coal
HST
TST
Dp
Wet Forest
6
1791
DOM
HST
TST
Dp
Open M oor
5
1794.6
Coal
HST
TST
Sh
Dry Forest
4
1798.3
Coal
HST
TST
M FS
Swamp Forest
3
1798.57
Coal
HST
TST
Dp
Limnic
2
1799.1
Coal
HST
TST
Sh
Terrestrial
1
1799.97
Coal
HST
TST
Sh
Limnic
5 4
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3
8-13-44-2W5
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EP T
06-07-40-20W4
12
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Coal
HST
HST
Sh
Terrestrial / Dry Forest
3
2277
Coal
HST
HST
Sh
Reed M oor
2
2279
Coal
HST
TST
Sh
Terrestrial
1
2289.5
Coal
HST
M FS
M FS
Limnic
5
918.5
Coal
HST
HST
Sh
Swamp Forest
4
919
DOM
HST
TST
M FS
Open M oor
3
935.2
Coal
HST
HST
Sh
Wet Forest
2
935.5
Coal
HST
HST
Sh
1
935.9
Coal
HST
HST
Sh
Terrestrial
Swamp Forest / Limnic
RI
15-08-63-05W5
4
PT
8-4-42-5W5
SC
Table 1 – List of the samples analyzed. For each sample it is indicated the 3rd and 4th -order depositional sequences system tracts and 5th -order eustatic sequence cycles where the relative
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coal layer formed, which was determined by means of facies analysis and sequential stratigraphic correlations (Fig. 2). The maximum flooding surface (MFS) indicates the
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maximum transgressive event. For each sample the depositional environment, defined
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interpreting the TPI and GI petrographical indices (Fig. 5 and Table 3), is also reported.
ACCEPTED MANUSCRIPT
Wells
10-25-4025W4 27 5.5
9-11-3717W4 95 19.5
14-29-4523W5 70.8 7.95
10-36-3922W4 26 7.5
06-07-4020W4 18.4 5.6
8-13-442W5 30.2 1.8
8-4-425W5 22.8 0.8
15-08-6305W5 36.2 1.4
Average
ST Thickness (m)
8
27.5
25
4.4
10.7
9.1
2.8
24.8
14.04
Coal cumulative Thickness (m)
3
6
8
0.4
3.7
0
0.4
1.4
2.86
Proportion in respect to the Total Coal thickness (%)
54.5
30.8
100
5.3
66.1
0
50
100
50.84
Proportion in respect to the ST thickness (%)
34.6
0
14.3
5.6
19.36
0
0.2
0.35
1.05
12.7 1.8
1.1 0.4
8.1 0
16.51 3.25
Total stratigraphic thickness (m) Total Coal thickness (m) HST
TST
LST
37.5
21.8
32
9.1
M ean coal layer Thickness (m)
3
1.2
1
0.4
ST Thickness (m) Coal cumulative Thickness (m)
15.5 2.5
61.5 13.5
8.3 0
18.6 7.1
Proportion in respect to the Total Coal thickness (%)
45.5
69.2
0
Proportion in respect to the ST thickness (%)
16.1
22
M ean coal layer Thickness (m)
2.5
2.3
ST Thickness (m)
3.5
6
Coal Thickness (m)
0
Proportion in respect to the Total Coal thickness (%)
0 0
M ean coal layer Thickness (m)
E C
U N
6.3 0.7
94.7
12.5
100
50
0
46.49
38.2
11.1
14.2
36.4
0
17.25
2.4
0.4
0.3
0.2
0
1.13
38
3
1.4
8.4
18.9
3.3
10.31
0
0
1.2
0
0
0
0.15
0
0
0
21.4
0
0
0
2.68
0
0
0
85.7
0
0
0
10.71
D E
T P
Proportion in respect to the ST thickness (%)
I R
C S 1.2
T P
0
A M 0 1
1.2
Table 2 – Thickness of the coal layers in the 4th -order depositional sequences system tracts calculated for each core analyzed
C A
40.80 6.26
1.2
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Index
Macerals Rate
Variable
Vs/Vd
Telinite+Collotellinite/Collodetri nite+Vitrodetrinite
Environmental information
Structured versus detrital organic
Vegetation Type and Degradation process
matter Semifusinite/Fusinite
Degree of oxydation in the peat
Dryness and exsposition rate
V/I
Vitrinite/Inertinite
Rate of humidity in the peat
High/Low water table
T/F
Total Vitrinite/Fusinite+Semifusinite
Rate of Gelified/Fusinized of the
Wet Forest/Dry Forest
organic matter
TPI
GI
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vegetation
Forest-moor versus reed-more vegetation
Degradation/Transportation processes Type of vegetation
Type of vegetation and degradation processes
Forest versus marsh vegetation
Type of vegetation
Rate of Gelified/Fusinized of the
Wet/Dry conditions
organic matter
Telinite+Collotellinite+Fusinite+ Forest versus marsh vegetation Semifusinite+Suberinite+Resinit e/ Collodetrinite+Inertinite+Sporini te
Type of vegetation
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VI
Forest-moor versus reed-more
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S/D
Structured/detrital inertinite
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W/D
Semifusinite+Fusinite/Inertodetri nite+M acrinite+M icrinite Telinite+Collotellinite+Fusinite+ Semifusinite / Alginite+Sporinite+Inertidetrinit e Telinite+Collotellinite+Fusinite+ Semifusinite / Alginite+Sporinite+Inertodetrinit e+Collodetrinite+Vitrodetrinite Telinite+Collotellinite+Fusinite+ Semifusinite / Collodetrinite+M acrinite+Inertod etrinite) Total Vitrinite+M acrinite/Semifusinite +Fusinite+Inertodetrinite
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IR
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SF/F
Table 3 – Petrographic indices calculated in this work and information provided by their use
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(From Calder et al., 1991; Diessel, 1986; Kalkreuth and Leckie, 1989).
ACCEPTED MANUSCRIPT HST
M FS
39
8
29.29
40.33
65.33
C (%, Dry bases)
56.05
45.18
24.46
STot (%, Dry bases)
1.28
2.53
0.73
Vitrinite (%)
42.7
45.5
27.8
52.5
66
71.3
32.6
17
6.5
40
24.6
16.7
6.1
6.4
4.7
7.5
9.3
12.1
18.6
31.1
61
Mineral Matter Free-basis (%) Inertinite (%) Mineral Matter Free-basis (%) Liptinite (%) Mineral Matter Free-basis (%) M ineral M atter (%)
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Ash (%)
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N. samples
TST
Table 4 - Average of the most relevant petrographic and geochemical data for each 4th -order
Dry Forest
19
20
58.66 29.24
C (%)
58.51
S (%)
1.15
Wet Forest
Swamp Forest
Reed M oor
Limnic
Open M oor
7
10
7
8
35
70.56 12.30
51.77 34.52
69.66 13.67
68.69 12.31
69.84 10.99
21.24 70.57
69.55
49.79
67.54
69.77
71.57
19.36
1.83
2.39
2.90
2.01
1.49
1.43
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TOC (%) Ash (%)
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Terrestrial
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Number of samples
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depositional sequence system tract
HI (mgHC/gTOC)
150.16
159.80
145.00
185.50
178.71
237.00
150.77
OI (mgCO2/gTOC)
13.60
18.71
17.76
15.93
18.57
15.89
14.62
Vitrinite (%)
21.79
67.17
73.39
62.79
75.43
21.88
54.00 38.12
76.55 15.50
81.22 12.20
65.99 27.77
82.70 11.03
65.42 5.39
65.76 9.36
40.43 5.26
17.67 5.07
13.50 4.77
29.19 4.59
12.09 4.75
16.12 6.01
M ineral M atter (%)
10.29 9.00
5.57 5.73
5.78 12.26
5.28 9.64
4.82 4.86
5.21 8.80
17.97 66.55
Vs/Vd SF/F
0.31 7.53
1.05 5.70
3.64 5.56
1.95 7.85
0.47 5.88
0.71 4.54
-
3.31
8.91
8.48
5.96
3.68
8.01
-
0.39 1.70
1.43 1.81
15.97 17.66
16.22 27.30
2.29 3.00
9.81 12.14
-
W/D S/D
4.44 0.87
7.34 1.58
14.46 2.64
32.94 1.83
5.02 0.79
13.59 0.83
-
TPI GI
0.91 0.42
1.80 1.50
4.12 16.20
2.11 21.13
0.83 2.37
0.91 10.14
-
VI
0.89
1.62
2.71
2.02
0.79
0.86
-
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50.91
23.95 59.84
Min.Matt. Free-basis (%) Inertinite (%) Min.Matt. Free-basis (%)
IR V/I T/F
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Liptinite (%) Min.Matt. Free-basis (%)
Table 5 - Average of the most relevant geochemical and petrographical data of each coal depositional environment.
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SC
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ACCEPTED MANUSCRIPT
ACCEPTED MANUSCRIPT Appendix 1 – Maceral analysis data Appendix 2 – Petrographic indices calculated on the samples containing more than 50% of organic matter (coal)
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Appendix 3 – Elemental Analysis data
Silvia Omodeo Salé, Rémy Deschamps, Pauline Michel, Benoit Chauveau, Isabel Suárez-Ruiz PII: DOI: Reference:
S0166-5162(17)30095-2 doi: 10.1016/j.coal.2017.05.020 COGEL 2847
To appear in:
International Journal of Coal Geology
Received date: Revised date: Accepted date:
2 February 2017 30 May 2017 31 May 2017
Please cite this article as: Silvia Omodeo Salé, Rémy Deschamps, Pauline Michel, Benoit Chauveau, Isabel Suárez-Ruiz , The coal-bearing strata of the Lower Cretaceous Mannville Group (Western Canadian Sedimentary Basin, South Central Alberta), part 2: Factors controlling the deposition of organic matter accumulations. The address for the corresponding author was captured as affiliation for all authors. Please check if appropriate. Cogel(2017), doi: 10.1016/j.coal.2017.05.020
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ACCEPTED MANUSCRIPT The Coal-bearing strata of the Lower Cretaceous Mannville Group (Western Canadian Sedimentary Basin, South Central Alberta), Part 2: Factors controlling the deposition of organic matter accumulations.
Silvia OMODEO SALÉ1 , Rémy DESCHAMPS1 , Pauline MICHEL1 , Benoit
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CHAUVEAU1 and Isabel SUÁREZ-RUIZ2
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(1) IFPEN, 1 & 4 Avenue du Bois-Préau, 92852 Rueil-Malmaison cedex – France
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(2) INCAR – CSIC, c./ Francisco Pintado Fe, 26, 33011 Oviedo - Spain
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Corresponding author: [email protected]
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Abstract
This work analyzes the distribution of coal-bearing strata in the stratigraphic framework of the
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Mannville Group (Lower Cretaceous, Western Canada Sedimentary Basin). In the 3rd -order depositional sequence the maximum abundance of coal layers is found in the highstand system
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tracts (HST), whereas in the 4th -order eustatic sequences, coal deposits distribute similarly in the highstand and transgressive system tracts (TST). These trends have been related to the variation
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of accommodation space in the basin, which mostly influence the occurrence of favorable conditions for organic matter preservation. Petrographic analyses permit to identify variation in the coal layers composition and to relate them with the stratigraphic dynamic of the basin. The HST is characterized by a low subsidence rate, which induces low levels of the groundwater table, favoring dry conditions in the peat. By consequence, in the HST a higher abundance of inertinite maceral group is observed than in the TST. On the other hand, the TST is characterized by higher subsidence rates, thus more stable groundwater table levels, promoting the organic matter preservation. Therefore, in the TST a higher content of vitrinite and liptinite maceral groups is observed. In correspondence of the
ACCEPTED MANUSCRIPT maximum flooding surface (MFS), the peat is frequently flooded, with the consequent dilution of the organic matter with terrigeneous sediment, forming carbonaceous shales deposits. By the analysis of the organic matter composition, seven depositional environments for coal were identified, located at different distance from the coast line. Each depositional environment is characterized by a specific organo-facies association, which is the reflex of different
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environmental conditions in the peat, in terms of water table level, type of vegetation and hydrodynamic processes. The vertical superimposition in a coal package of different
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depositional environments has been related to high order climatic cyclicity (5th -order
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transgressive and regressive cycles), which controls the groundwater table fluctuations.
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Highlights
Distribution of the coal deposits in the stratigraphic framework
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The organic matter preservation is controlled by the accommodation space The depositional environments where coal forms are defined
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High order climatic cyclicity induces compositional changes in the coal beds
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Keywords: coal; macerals analysis; petrographic index; Mannville Group; accommodation
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space; groundwater table
1. INTRODUCTION Accumulation of organic matter can be found in a very large variety of depositional environments, from continental to marine. However, only in few cases the environmental conditions are favorable for the preservation in the sediment of great amount of organic matter to form coal deposits and/or hydrocarbons source rocks (Bordenave, 1993; Taylor et al., 1998). Different types and amount of organic matter can be deposited, depending on the type of producers, the proximity to the coastline, the river drainage, the redox conditions of the depositional environment and the residence time in the degradation zone (including oxidation reactions but also reduction processes) (Arthur and Sageman, 1994; Berner and Canfield, 1989;
ACCEPTED MANUSCRIPT Bralower and Thierstein, 1984; Burdige, 2007; Tyson, 2001). This work aims to improve the understanding of the formation of deposits containing abundant organic matter, which form in the alluvial to the coastal-tidal plains depositional settings. These deposits have a relevant economic interest, because they can form coal deposits and gas-prone source rocks (carbonaceous shales mostly formed by Type III kerogen). Thus, understanding the processes of
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formation, distribution and composition variation of these types of rocks in the basin is of great scientific and economic interest. To achieve the objective proposed in this work, the coal beds
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forming the Mannville Group deposits (Lower Cretaceous, Western Canada Sedimentary Basin,
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Alberta, Canada) were analyzed.
The conditions required to form carbonaceous rocks are mainly: 1) the presence of important
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sources of organic matter during deposition and 2) the setting of favorable condition for organic matter preservation during the geological history of the basin (Taylor et al., 1998). The
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preservation of the coal layers is strictly controlled by the position of the water table relative to the surface, which is influenced by the accommodation rate, the eustatic variations and the
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rainfall rate in the peat (Banerjee et al., 1996; Bohacs and Suter, 1997; Holz et al., 2002). The groundwater table level controls the degree of humidity in the soil, thus the type of vegetation
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produced and accumulated and the diagenetic gelification processes. The combination of these factors determines the organo-facies characterizing the coal deposits (e.g. Banerjee et al., 1996; Cross, 1988; Chalmers et al., 2013; Diessel et al., 2000; Flint et al., 1995; Gastaldo et al., 1993;
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Teichmüller and Teichmüller, 1982; Wadsworth et al., 2002, 2003). Hydrologic regimes characterized by low water level determine frequent oxidation and degradation of the organic matter formed in the peat, whereas very high groundwater levels can drown the mire and favors the deposition of relevant amounts of terrigeneous sediments. At the equilibrium point favorable conditions for the accumulation and the preservation of high content of well-preserved and structured organic matter (Diessel et al., 2000). A relationship between the environmental conditions of the ancient peat-forming ecosystems and the petrological composition of the organic matter preserved have been extensively inferred in the literature (e.g. Calder et al., 1991; Cohen et al., 1987; Chalmers et al.,
ACCEPTED MANUSCRIPT 2013; Davies et al., 2005; Diessel, 1982, 1986; Diessel et al., 2000; Diessel, 1992, 2007; Harvey and Dillon, 1985; Holz et al., 2002; Stach et al., 1982; Staub, 2002; Styan and Bustin, 1983; Teichmüller, 1989; Wadsworth et al., 2003; Wadsworth et al., 2010). Diessel (1982) was the first to propose a method to describe the organo-facies composition in coals, based on the definition of petrographic indices. The most relevant indices considered are i) the tissue
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preservation index (TPI) and ii) the gelification index (GI). The TPI index provides an indication of the presence of structured or unstructured materials and thus of the type of
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vegetation dominant in the peat. The GI index gives an indication of the humidity in the peat
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and thus of the degree of the dryness and of the groundwater table level. The petrographic indices proposed have been used to reconstruct facies diagrams (Diessel, 1986), where each
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field represents the combination of specific environmental conditions. Diessel’s indices were used, modified and integrated by several authors (e.g., Calder et al., 1991; Nicolas et al., 1997;
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Petersen, 1993), improving the interpretation of the environmental conditions where TOM forms in different geological contexts and areas.
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In the past, several studies have been specifically carried out to link the maceral composition of the Mannville Group coal deposits with the paleo-environments of the peat
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where they have been formed (Kalkreuth and Leckie, 1989; Kalkreuth et al., 1991; Lamberson et al., 1991; Marchioni and Kalkreuth, 1991), with the main scope to differentiate the compositional characteristics of the coal formed in the strandplain in respect to the delta plain
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settings. Herein, the sub-depositional environments where the Mannville Group coal deposits formed are analyzed in detail, by means of organo-facies analysis and the interpretation of petrographic indices. The distribution of these sub-depositional environments in the stratigraphic framework was also determined, trying to understand the link between coal composition with the groundwater table fluctuation, which is in turn related to the interaction among the different orders transgressive/regressive cyclicities.
2. GEOLOGICAL SETTING
ACCEPTED MANUSCRIPT The Western Canada Sedimentary Basin (WCSB) is a northeast-southwest major clastic wedge of the foreland basin derived from the Cordillera. It extends from the Cordillera foreland thrust belt towards the Canadian Shield and it covers an area of approximately 2 million km2 (Fig. 1). The thickness of the wedge reaches its maximum at the east of the foothills front, at the axis of the Alberta Syncline (about 6000 meters) and it decreases in the northeast direction,
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towards the Canadian Shield (Strobl, 1988). The infill of the WCSB resulted from two tectonic phases (Cant and Abrahamson, 1996). In the first Paleozoic-Jurassic phase, it formed a
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succession dominated by carbonate sedimentation and deposited on the top of the stable craton,
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next to North America's earlier passive margin. In a second mid-Jurassic-Paleocene phase, a context of foreland basin was instated. The foreland succession overlaid the previous carbonate
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deposits and mainly consists of clastic deposits, coming from uplifted Canadian Cordillera. Following these two successions, during the Paleocene, net erosion and sediment by-pass have
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prevailed in the area. In the second tectonic phase, as the North American plate started to drift westward with the opening of the Atlantic ocean, the western margin of the continent suffered at
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least two major compression episodes, which led to uplift of thrusted and folded rocks that formed the Canadian Rocky Mountains. As a consequence of this tectonic activity, the foreland
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was subject to two distinct subsidence phases, from Late Jurassic (Oxfordian) to Early Cretaceous and from the Middle Cretaceous (Aptian) to Eocene, separated by a major unconformity (Cant and Abrahamson, 1996). The Mannville Group was deposited on these
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unconformities, overlying tilted and truncated strata ranging from the Paleozoic to the Mesozoic Eras (Cant and Abrahamson, 1996; Jackson, 1984). The Mannville Group deposited during Barremian-Aptian to Early Albian Stage (+/- 120 to 104 My) and it blanketed the entire Western Canadian foreland basin, with a thickness ranging from less than 40 meters eastward to more than 700 meters in the Rocky Mountain Foothills. In the study area (Fig. 1) thickness ranges from 95 to 320 meters (Hayes et al., 1994). The entire Group corresponds to a third-order sequence (Cant and Abrahamson, 1996), bordered at the top and at the bottom by tectonically generated unconformities. The Lower Mannville strata corresponds to the lowstand system tract (Jackson, 1984) and it consists of fluvial sediments
ACCEPTED MANUSCRIPT that change upward into marginal marine deposits (estuarine to tidal and shoreface deposits) and are sealed by offshore marines shales corresponding to the maximum flooding surface (MFS) of the same order sequences (Cant and Abrahamson, 1996; Langenberg et al., 1997). The latter transgressive deposits are considered as part of the informal “Middle Mannville”. The Upper Mannville deposits correspond to the highstand system tract (Jackson, 1984) and it is a
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succession of shallow marine sediments that progressively change into fluvial, coastal plain and floodplain facies. The Upper Mannville encompasses a set of successive progradations across
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the whole basin, in a northward direction. Generally marine shale deposits are found in the
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north, shoreface sandstones in the central part of the basin and continental deposits are deposited in the south (Cant and Abrahamson, 1996). In the entire Manville Group several coal
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deposits have been identified, with a maximum abundance in the Upper Mannville. Coal layer extended throughout the entire basin, with lateral extension up to more than 300 km and vertical
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thickness from 1 to 10 meters.
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3. METHODOLOGY
Eight cores representative of the Middle-Upper Mannville Group deposits were selected
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(Fig. 2). These cores represent the stratigraphic record of eight wells located along the geological cross-sections reconstructed by Deschamps et al., (in press). The stratigraphic record of each core was described by means of facies analysis and it was subdivided in 4 th -order
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depositional sequences, with definition of the related lowstand (LST), transgressive (TST) and highstand (HST) system tracts (Fig. 3). To determine the features of the Mannville Group coal deposits, a total of 106 samples were collected, each one representing a single point in the cores (Table 1) and analyzed by means of petrographic and geochemical analyses. Samples were formed by both coal (Carbon content, C >50%) and carbonaceous shales (C <50%). To quantify the relative abundance of the coal in the 4th -order system tracts, the cumulative thickness of the coal measured in the HST, TST and LST system tract, forming each depositional sequence, in respect to the total cumulative coal thickness measured in the total
ACCEPTED MANUSCRIPT core was determined (Table 2). To normalize this data, for each system tract, the proportion of the coal cumulative thickness relative to the total sediment thickness was also determined.
3.1. Petrographic Analyses The petrographic analyses were performed at the Petrography laboratory of the INCAR
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(Oviedo, Spain). Petrographic pellets were prepared for petrographic analysis according to the standard procedure described in the ISO-7404-2 (2009) norms. The maceral analysis was
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carried out on the coal and shaly coal samples (formed by dispersed organic matter – DOM),
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based on 500 counts per sample (Appendix 1). The analysis was performed using reflected MPV-Combi-Leitz optical microscope with an oil immersion objective (50x) and with a point-
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counter coupled to the microscope. Incident white light was used, together with fluorescence mode when necessary, after excitation with UV and blue-violet light under a Leica DM 4500P
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microscope. Maceral analysis determines the relative proportion of the macerals in the sample. Mineral matter was included in the count. Maceral classification was determined according to
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the (ISO-7404-2, 2009) norms and using the last established maceral classification defined in ICCP (1998; 2001), Sýkorová et al. (2005) and Pickel et al. (2016).
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The results of the maceral analysis were used to calculate petrographic indices proposed in the literature (Diessel, 1986; Kalkreuth and Leckie, 1989) (see Table 3 for indices explication and Appendix 2 for indices results). Petrographic indices provide information on: 1) the
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humidity rate in the peat (SF/F, T/F, and GI indices); 2) the vegetation type (ligneous or herbaceous) (W/D, S/D, TPI and VI indices); 3) the intensity of the degradation/preservation processes (Vs/Vd, IR and S/D indices) and 4) the influence of the groundwater table (V/I and GWI) (Table 3). Indices were calculated only on the samples containing more than 50% of organic carbon. In the case of the samples formed by carbonaceous shales petrographic indices were not determined, because organic matter fragments were too small for maceral classification. Thus, only the proportions of vitrinite, inertinite and liptinite maceral groups were defined for these samples. The integration of the data provided by the different indices permits to describe the environmental conditions prevailing at the time of peat accumulation.
ACCEPTED MANUSCRIPT To reconstruct the depositional environments where the organic matter accumulated, the facies diagram proposed by Diessel (1986) and modified by Nicolas et al. (1997) was used. In this diagram variations of the TPI (tissue preservation index) and GI (gelification index) indices (Diessel, 1986) identify 6 fields, each one representing different environmental conditions of the peat, in terms of humidity rate, frequency of the groundwater table oscillations, type of
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vegetation and preservation/degradation processes. The combination of these properties defines specified organic matter depositional environments. Thus, an organic matter depositional
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environment was determined for each sample. In the case of the samples whose indices were
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projected in the intersection of the fields of two depositional environments, both depositional
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environments were considered (Fig. 4).
Proximate and Ultimate Analyses
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Moisture, ash, and volatile matter contents were obtained (Appendix 3), according to the ASTM-D7582-10 (1981) and ISO-562 (1998) standards. For the same subset of samples, the C,
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H, N, and total sulfur contents were determined using a LECO CHN 2000 and a LECO S632 apparatus, according to the ASTM-D5373-08 (2008) and ASTM-D4239-08 (2008). Analyses
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were carried out on samples crushed to less than 212 µm. The determination of C and Ash discerns coal (C > 50%) from the shaly coal and coaly shale deposits (C < 50%), formed by
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dispersed organic matter (DOM) in the mineral matrix.
4. RESULTS
4.1. Thickness and properties of the coal layers in the 4 th-order eustatic sequences The frequency of occurrence of the coal layers in the 4th -order eustatic sequences and the proportion of the coal thickness in respect to the total thickness of each system tract was calculated for the eight cores (Table 2). The average of the values obtained for the eight cores indicate that the 51% of the coal layers formed in the HST, the 46% in the TST and the 3% in the LST. In several cases the maximum flooding surface (MFS) of the 4 th -order eustatic sequences, which marks the transition between the TST and the HST, passes throughout the
ACCEPTED MANUSCRIPT coal layers. The coal deposits form the 19% of the total system tract thickness in the HST and the 17% in the TST. Coal layers have an average thickness of nearly 1 meter in both system tracts. In the case of the LST, frequency was not calculated, as there is only one data point. A synthesis of the petrographical and geochemical characteristics of the coal layers formed in the different 4th -order system tracts is presented in Table 4. Data were obtained calculating
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the average of the values measured, by proximate and ultimate Analyses and maceral analysis, in the samples forming part of each system tract. Samples collected in correspondence of the
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MFS were considered separately. The content of organic carbon (C) is similar in the coal layers
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composing the HST (56%) and the TST (45%). The lowest content of C (%) is measured in the samples collected at the MFS (average of 24%), as herein mostly form dispersed organic matter
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deposits (DOM). The highest contents of ST are measured in the samples formed in the TST (2.5%).
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The petrographic composition of the coal deposits was determined considering the average percentage of the three maceral groups (vitrinite, inertinite and liptinite) counted in the samples
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representing each 4th -order system tract (Table 4). Mineral matter-free data indicate that the vitrinite is the most abundant maceral group in both TST and HST (53% and 66% respectively).
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The inertinite maceral group is more abundant in the HST (40%) than in the TST (27%) and the liptinite maceral group is more abundant in the TST (9%). The highest content of mineral matter is found in the layers formed in correspondence of the MFS (61%), which in most of the case
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constitute carbonaceous shales. A higher content of mineral matter is contained in the coal deposits formed in the TST (31%) than in the HST (19%).
4.2. Definition of higher order cycles in the coal packages Centimetric to metric packages of coal can be found along the entire Upper Mannville Group stratigraphic record. Petrographic observations evidence relevant differences in terms of maceral composition in the samples collected in a same package. The calculation of petrographic indices helped to describe and to understand these variations (Table 3). Vs/Vd, IR, W/D, S/D, TPI and VI indices >1 generally indicate a good preservation of the vegetal tissues
ACCEPTED MANUSCRIPT and the dominance of forest vegetation, whereas lower values (< 1) indicate a poor preservation of the vegetal tissues and the dominance of swamp, marsh and grass vegetation (Diessel, 1986; Kalkreuth and Leckie, 1989). High SF/F, T/F and GI indices suggest wet conditions in the peat, whereas low values indicate dry conditions. High Vs/Vd, IR and S/D indices indicate a good preservation of the organic matter, whereas low values suggest a degraded and bracket state
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(Diessel, 1986; Kalkreuth and Leckie, 1989). Variations of the petrographic indices along a same package (Fig. 2 and Appendix 2) allow
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high order cycles (5th order) to be individually identified (Fig. 3), which can correspond to
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regressive and transgressive events induced by high order climatic oscillations (Chalmer et al., 2013, Wadsworth et al., 2010). Deepening cycles (DP) are generally formed by organic matter
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which petrographic indices indicate the dominance in the peat of wet conditions (high SF/F, T/F and GI indices), the presence of vegetation formed by arborescent plants (Vs/Vd, IR, W/D, S/D,
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TPI and VI indices >1) and good preservation conditions (high Vs/Vd, IR and S/D indices). The shallowing cycles (SH) are represented by organic matter whose petrographic indices indicate
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drier conditions in the peat (low SF/F, T/F and GI indices), the dominance of shrub, grass and detrital vegetation type (Vs/Vd, IR, W/D, S/D, TPI and VI indices <1) and relevant oxidation
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and degradation of the organic matter (low Vs/Vd, IR and S/D indices). Passing from the SH to the DP cycles, an increase of the mineral matter content was frequently observed (Fig. 2 and
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Appendix 2).
4.3. Coal depositional environments Plotting the TPI (Tissue Preservation Index, rate between the structured and unstructured macerals) and the GI (Gelification Index, rate between gelified and oxidized macerals) indices on the facies diagram proposed by Diessel (1986) and modified by Nicolas et al. (1997) (Fig. 4), the environmental conditions where the peat forms are defined for each sample (Fig. 3). High TPI values indicate large amount of well-preserved plant tissues and are interpreted to reflect the abundance of arboreal vegetation (wood-derived macerals). Low TPI values indicate higher degradation of the organic matter and relevant contribution of detrital woody matter. High GI
ACCEPTED MANUSCRIPT indicates high humidity rate in the peat, due to high groundwater table levels, which allows the gelification processes to develop extensively. On the contrary, low GI values indicates dryer conditions, which favored the oxidation of the organic matter. The combination of these indices permits identification of six coal depositional environments: Terrestrial, Dry Forest, Wet Forest, Swamp Forest, Limnic and Reed Moor. An additional depositional environment was proposed
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herein (Open Moor), describing a limnotelmatic setting where shaly coal and coaly shale formed (C < 50%) (Wadsworth et al., 2010). In this latter depositional environment mixed terrestrial
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and marine organic matter deposited.
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The distribution of the proposed depositional environments in the alluvial and coastal plains is shown in Fig. 5. The environmental conditions and the preservation processes dominating in
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these settings were constraint interpreting the petrographic indices and the microscopic features
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observed. A synthetic overview of those environments is given in Figs. 6-9 and Table 5.
4.4. Occurrence of the coal depositional environments in the stratigraphic framework
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The percentage frequency of occurrence of the defined coal depositional environments in the 4th -order system tracts was determined (Fig. 10). In the case for a same samples the TPI and
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GI indices were projected in the intersection of two fields, both depositional environments were counted. Therefore, the sum of the frequency of distribution of the seven depositional environments defined is nearly higher than 100% (Fig. 10).
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The Terrestrial and Dry Forest depositional environments form mostly in the HST; the Wet Forest and Swamp Forests depositional environments in the TST and at the TST-HST transition, in correspondence of the MFS; the Reed Moor depositional environment forms mostly in the HST; the Limnic depositional environment in the TST and in correspondence of the MFS; the open moor forms mostly in the MFS and secondarily in the TST. Therefore, in the HST form with higher frequency the Terrestrial, the Dry Forest and the Reed Moor depositional environments (Fig. 10). In the TST a more uniform distribution of the coal depositional environments is observed. The Terrestrial and Dry Forest depositional environments are the less
ACCEPTED MANUSCRIPT represented. The samples collected at the MFS are formed mostly in the Open Moor depositional environment (Fig. 10).
5. DISCUSSION 5.1. Coal deposits in the stratigraphic framework
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The variation of the accommodation space in the terrestrial setting is expressed by the fluctuation of the groundwater table, which in turn is induced by the different orders regressive
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and transgressive cycles recorded in the basin (Bohacs and Suter, 1997; Wadsworth et al., 2002,
SC
2003). At the 3rd -order cyclicity, the most numerous coal layers form in the highstand system tract (HST) and particularly in the early to middle part (Fig. 2) (Deschamps et al., in press). At
NU
this time the rising of the groundwater table is stable low enough for favoring vertical and lateral peat accumulation (Bohacs and Suter, 1997, Wadsworth et al., 2003). Differently, at the
MA
4th -order cyclicity, coal distributes with similar proportion and layer thickness in the TST and in the HST (Table 2). This observation is confirmed by the proportion of the coal layers in respect
ED
to the total thickness of sediments, which indicate the preservation of similar abundance of organic matter in both HST and TST (Table 2). This different trend, in respect to what was
EP T
observed in the 3rd -order depositional sequences, may be the consequence of the lower variation of the accommodation space at 4th -order, which permits to maintain favorable condition for organic matter preservation in both HST and TST. By contrast, very little organic matter is
AC C
observed in the 4th -order LST, suggesting that at this stage the accommodation rate was generally lower than the production rate, with consequent lower groundwater table levels, favoring the erosion of the peat and avoiding the preservation of the organic matter. The geochemical signal of the organic matter formed and preserved in the 4th -order HST and TST is very similar (Table 4). The only relevant difference is the proportion of total sulfur content (evaluated in %), which is contained in higher proportion in the TST (Appendix 3). This trend can be related to the influence of sea-water during the transgressive periods (high sea level), which favored the formation of pyrite in the peat.
ACCEPTED MANUSCRIPT Variation in the organic matter composition is detected by petrographic analyses. A relationship between the type of organic matter accumulated in the peat and the eustatic and accommodation space cycles has been proposed in the literature (Banerjee et al., 1996; Chalmers et al., 2013; Davies et al., 2005; Diessel et al., 2000; Wadsworth et al., 2002, 2003). The regressive and transgressive cycles have a direct influence on the hydrologic regimes
PT
(groundwater table oscillations), which determine variation in the environmental conditions in the peat and thus of the organic matter accumulated. In the 4th -order eustatic sequences of the
RI
Mannville Group high content of the inertinite maceral group is measured in the HST (Table 4),
SC
indicating the dominance in this eustatic regime of dry and oxidized environmental conditions in the peat. The latter may be a consequence of the low accommodation space formed in the
NU
HST, which determine low levels and/or high fluctuation of the groundwater table. On the other hand, in the TST the vitrinite maceral is very abundant and well preserved, and it is frequently
MA
associated with liptinite. This composition reflects the maintenance in the transgressive periods of high water levels of the groundwater table, which favors the gelification and preservation of
ED
the organic matter and the deposition of aquatic origin (rich in lipids). At the MFS dominate the formation of carbonaceous shales, as very high levels of the groundwater table are reached,
EP T
determining the “long-term” drowning of the mire and the deposition of relevant amounts of terrigeneous sediments.
Maceral analysis reveals high organic-facies heterogeneity along package of organic matter
AC C
rich-deposits formed in a same cycle (Fig. 3). This heterogeneity can be observed at very low scale (deci-metric to cent-metric) and it is evidenced by variation of the petrographic indices (Appendix 2).
The distribution of the petrographic indices along the stratigraphic record indicates a cyclicity in the organo-facies associations and thus in the environmental conditions of the peat. Therefore, it can be suggested that the variation of the organo-facies associations in a same package is induced by high order eustatic/climatic cyclicity (5th order or higher) that determines the shift of the coast line during the time and the oscillation of the groundwater table. The latter determines variation over time of the humidity rate and thus on the vegetation type and on the
ACCEPTED MANUSCRIPT gelification/oxidation processes. Similarly to what was observed in the 4th -order eustatic sequences, 5th -order shallowing-regressive cycles are associated with organo-facies association of dry conditions and frequent exposition of the peat, whereas in the deepening-transgressive cycles organo-facies indicative stable wet conditions.
PT
5.2. Formation of the coal depositional environments The maceral associations found in an organic matter-rich layer are related to the
RI
characteristics of the depositional setting where it was deposited. Therefore organo-facies have
SC
been associated with specific sub-depositional environments that form in the alluvial and deltatidal plains (Calder et al., 1991; Cohen et al., 1987; Chalmers et al., 2013; Davies et al., 2005;
NU
Diessel, 1982, 1986; Diessel et al., 2000; Diessel, 1992, 2007; Harvey and Dillon, 1985; Holz et al., 2002; Stach et al., 1982; Staub, 2002; Styan and Bustin, 1983; Teichmüller, 1989;
MA
Wadsworth et al., 2003; Wadsworth et al., 2010). These sub-depositional environments are located at different distance from the coast-line, which determines a different dynamic of the
ED
precipitation, evaporation and infiltration processes. The combination of these parameters is reflected in the groundwater table level, which in turn determines the rate of humidity in the
EP T
peat and thus the type of vegetation (Bohacs and Suter, 1997; Moore and Shearer, 2003). The oscillation of the groundwater table influences also the preservation state of the organic matter, as
frequent
fluctuations
cause
the
exposition
and
oxidation
of
the
peat.
The
AC C
preservation/degradation of the organic matter in the peat is additionally related to the energy of the fluvial, tidal and waves processes, which determines the intensity of the transport and the erosion of the organic matter and also the supply in the peat of terrigeneous material. The energy of the depositional setting is strictly linked to the position along the sedimentary profile. Therefore the position where it is located the peat in the alluvial-delta plain, determine the type of organic matter deposited (Fig. 5). The Terrestrial depositional environment is located in the most alluvial plain landward position (Fig. 5). At this point, frequent oscillations of the groundwater table are suggested, which cause continuous exposition of the peat. Thus, organic matter can be easily reworked by
ACCEPTED MANUSCRIPT meteoric agents and by fluvial transportation, giving as result a high fragmentation and oxidation of the vegetal tissues, frequently mixed with relevant amount of mineral matter (Fig. 6a-d). In the distal part of the alluvial part forms the Dry Forest depositional environment. In this environment the organic matter is well preserved and it is formed mostly by high plant remains (Fig. 6e-h). Thus, in respect to the Terrestrial depositional environment, a groundwater
PT
table more stable and a lower energy conditions are suggested for this environment, which permit the development of a high plants forest. However, the high oxidation of the organic
SC
conditions, thus of low levels of the groundwater table.
RI
matter (Fig. 6g and h) indicates the dominance also in this depositional environment of dry
In the proximal part of the upper delta plain forms the Wet Forest depositional environment
NU
(Fig. 5). In this environment organic matter is very well preserved and formed mostly by high plant tissues. Thus, a stable and relatively high level of the groundwater table is suggested,
MA
which favors the gelification and preservation of the organic matter (Fig. 7a-d). In the seaward position of the upper delta plain forms the Swamp Forest depositional environment (Fig. 5). In
ED
this environment the organic matter is formed mostly by remains of shrub vegetation, whereas high plants decrease. The abundance of aquatic-affinity macerals (e.g. alginite) and the
EP T
abundant mineral matter alternated with the organic matter (Fig. 7e-h), indicate more aquatic conditions in respect to the previous depositional environment. Thus, higher level of the groundwater table is suggested.
AC C
In the lower delta plain and in the interdistributary fluvial channels areas, the Reed Moor depositional environment (Fig. 5) is formed. The organic matter formed in this environment is mostly made up of shrub and grass vegetation remains, whereas high plants rest are less common. The increased energy in this part of the sedimentary profile of the tide, fluvial and wave currents makes unfavorable the development of high plants vegetation. In this environment, strong fluctuations of groundwater table occurred, which determine alternation of dry and wet condition and of exposition and flooded of the peat (Fig. 8a-d). In the delta plain shallow lakes, ponds and other aqueous environments from freshwater to hypersaline can be formed. In these environments forms the Limnic depositional environment (Fig. 5),
ACCEPTED MANUSCRIPT characterized by a stable and high groundwater table.. Swamp/shrub vegetation and aquaticaffine organic matter dominates, whereas high plants do not frequently develop. The organic matter is frequently alternated with terrigeneous material (Fig. 8e-h), which indicates a periodic flooding of the peat. In the distal part of the lower delta plain, close to the coast line, the Open Moor depositional
PT
environment can be formed (Fig. 5). This environment is characterized by a constant very high level of the groundwater table, which determines a continuous and relevant input of terrigenous
RI
material in the peat (Fig. 9). In the low energy areas, conditions favorable for organic matter
SC
deposition can be cyclically replaced with flooded events, with a high terrigeneous sediment supply, forming deposits constituting by alternation of organic matter and mineral matter layers
NU
(Fig. 9a-d). In these deposits, aquatic organic components (mostly algae) are frequent (Fig. 9d and h). On the other hand, in the high energy areas, accumulation of organic matter fragments,
MA
included in a mineral matter matrix, can be formed (Fig. 9e-h). In the Open Moor depositional environment abundant pyrite is found (Fig. 9e), suggesting the proximity of the sea.
ED
The distribution of the coal depositional environments in the stratigraphic framework is strictly related to the dynamic of the groundwater table. The regressive periods are characterized
EP T
by low subsidence and by the shift of the coast line seaward. Thus, the formation of a reduced accommodation space and the low level of the groundwater table favour the formation in the 4th order HST of depositional environments located in the landward position and characterized by
AC C
dry conditions (Terrestrial and Dry Forest depositional environments) (Fig. 10). On the other hand, in the transgressive periods, the higher subsidence and the shift of the coast line landward permit the formation of high accommodation space and high level of the groundwater table. Therefore in the 4th -order TST the depositional environments characterized by wet conditions (Wet Forest, Swamp Forest, Limnic and Open Moor) are more frequently found (Fig. 10). Due to the high accommodation space of the transgressive periods, large fluctuations of the groundwater table are possible, which determines the setting of a larger variability of depositional environments (from Terrestrial to Open Moor) (Fig. 5).
ACCEPTED MANUSCRIPT The results presented in this work allows the characteristics of the organic matter deposited in a basin to be related to the factors that influence the stratigraphic evolution of a basin and the features of the related depositional settings, which are, among others: the accommodation space, the sediment supply, the climate, the precipitation and evaporation rate, the type of vegetation and the primary production. This type of data is necessary when wanting to predict the
PT
distribution and preservation of the organic matter in a stratigraphic framework of a basin. The results obtained herein represent the basis for future works that aim to model the deposition of
SC
RI
the terrestrial organic matter in a basin.
6. CONCLUSIONS
NU
The analysis of the Mannville Group stratigraphic record provides relevant data on the distribution of the coal and carbonaceous shales in the stratigraphic framework of a sedimentary
MA
basin and on the variation of its compositional and geochemical properties. A relevant condition to preserve the coal deposits in a sedimentary basin is the achievement of
ED
the equilibrium between the accommodation and the peat production rate. In the 3rd -order depositional sequence this equilibrium is reached in the early-middle highstand, where form the
EP T
thickest and more laterally continuous coal layers. In the 4th -order depositional sequences, coal deposits distribute similarly in the highstand and transgressive system tracts, indicating that equilibrium conditions were equally reached in these periods.
AC C
In the 4th -order depositional sequences, very similar geochemical properties were observed between the organic matter formed in the TST and HST. However, some relevant differences are determined by means of petrographic analyses. The inertinite maceral group is more abundant in the HST, indicating the dominance of drier conditions and low levels of the groundwater table. The liptinite maceral group is more abundant in the TST, as the groundwater table reaches high levels, favoring the deposition of aquatic macerals rich in lipids. The variation of the environmental conditions in the peat determines the great heterogeneity of the relative abundance of the macerals constituting the organic matter. These variations are induced by 5th -order cycles, which oscillation causes the shift of the coast line along the
ACCEPTED MANUSCRIPT sedimentary profile, determining variation in the humidity rate, the type of vegetation and the fluvial to coastal transportation and hydrodynamic processes in the peat. The combination of these elements are expressed by the variation of the groundwater table level, which can be considered as one of the most relevant factor controlling the organo-facies (maceral association) forming the coal deposits.
PT
In the alluvial to delta plain organic matter accumulates in different depositional environments, each one characterized by specific environmental conditions and thus, different organo-facies
RI
association. The environmental conditions characterizing each depositional environment are
SC
strictly related with the dynamic of the groundwater table and with the energy of the environment, which in turn are influenced by the different order regressive/transgressive cycles
NU
and from the distance from the coast-line. In the HST of the 4th -order depositional sequences occurred with more frequency the depositional environments characterized by dry conditions
MA
(Terrestrial, Dry Forest and Reed Moor), thus low levels of the groundwater table. On the other hand, in the TST dominate the depositional environments characterized by wet conditions (Wet
ED
Forest, Swamp Forest and Limnic), thus higher levels of the groundwater table. The larger variability in the TST is due to the higher accommodation space formed in this period, which
EP T
permits higher fluctuation of the groundwater table and, thus, the formation of different depositional environmental conditions. This study demonstrates that the prediction of the terrestrial organic matter signature at a basin-scale cannot be considered only through the
AC C
depositional settings, whereas it is necessary to take into account the dynamic of the groundwater table, which is in turn induced by regressive and transgressive cycles, thus related to local tectonic events and to climatic external forcing.
Acknowledgements This paper is part of a larger IFPEN research project, dedicated to the stratigraphic modelling of organic matter distribution at basin scale (DORS project). Authors would like to thank INCARCSIC (Oviedo, Spain) for providing lab equipment and material for the petrographic and
ACCEPTED MANUSCRIPT geochemical analyses. Finally we thank the two IJCG reviewers, whom revisions and suggestions have considerably improved the quality of the manuscript. Appendix 1 – Maceral analysis data
Well/ sample
Depth (m)
T elinit Collot Vitrodet Collo Corpo Geli Sporin Cutini Resini e elinite rinite detrini gelilin nite inite te te t. te
Subei nite.
Algini Liptodet Bitum Fusini Semifusi te rinite inite te nite
10-25-40-25W4 1.0
9.5
0.0
31.9
0.0
0.0
4.2
0.2
11
1559
7.3
0.4
0.0
27.4
0.0
0.0
2.3
0.0
10
1559.2
0.8
1.2
0.0
27.3
0.0
0.2
1.0
0.2
9
1559.6
0.0
6.8
0.6
14.6
0.0
0.4
2.6
0.2
1560
0.6
13.7
0.2
50.5
0.0
0.0
1.9
7
1560.5
10.4
8.2
0.0
45.3
0.0
0.0
1.2
6
1571.5
0.0
28.9
5.0
0.8
0.0
0.0
5
1573.9
0.6
4.9
2.2
2.4
0.0
0.0
4
1574.2
1.6
50.8
0.2
35.0
0.0
0.0
3
1574.6
0.4
10.7
0.2
28.8
0.0
0.0
2
1575
0.4
8.1
0.0
62.7
0.0
0.0
1
1575.8
0.4
49.1
0.8
22.6
0.0
0.2
1122.2
0.0
28.7
2.0
14.6
0.0
23
1127
0.4
24.7
0.6
40.3
22
1132.1
3.7
20.0
1.2
16.5
21
1132.45
17.5
9.4
19
1146.4
0.0
2.6
20
1146.8
0.2
23.6
18
1146.9
0.0
3.0
17
1149.35
12.5
18.7
16
1167.4
0.0
15
1167.8
0.0
14
1168.1
13
1168.6
0.0
0.0
31.7
1.3
0.0
0.0
0.0
0.4
0.0
0.0
0.4
0.0
5.0
42.2
0.0
12.2
50.3
0.2
0.0
0.0
0.4
0.0
6.4
31.4
0.0
0.6
0.0
0.0
1.2
0.0
0.0
0.0
0.0
4.0
18.9
0.0
0.0
0.0
5.3
23.7
0.0
0.0
0.0
0.2
1.4
0.0
0.0
1.0
0.2
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.8
0.6
0.8
0.6
0.0
0.0
0.0
0.0
0.4
6.0
NU
5.2
1.4
0.0
0.2
0.0
0.0
0.4
0.0
6.3
38.9
3.6
0.0
0.4
0.0
0.0
1.0
0.0
4.6
13.2
2.0
0.0
0.2
0.0
0.0
1.0
0.0
1.8
8.1
0.0
9.0
0.0
0.0
0.0
1.2
1.2
0.0
0.6
8.4
0.2
2.3
7.5
1.0
0.8
0.0
0.2
0.8
0.0
3.4
13.0
2.2
0.4
2.2
0.0
0.0
0.0
0.0
0.0
0.0
3.3
13.9
2.2
18.7
33.5
0.4
0.0
1.8
0.2
2.5
0.0
0.0
1.8
0.0
0.0
0.0
0.0
31.2
0.0
0.0
0.0
0.0
1.6
0.4
2.8
2.2
0.2
0.0
3.0
0.2
0.0
0.0
0.0
0.0
0.0
0.0
1.6
0.4
0.0
0.0
12.9
0.0
0.0
0.0
4.2
1.8
1.0
0.4
1.4
0.0
28.0
0.4
0.5
5.3
0.0
1.5
0.0
0.4
2.5
0.0
1.3
16.0
2.2
1.8
31.6
0.0
0.2
0.0
0.4
0.2
0.0
0.0
0.0
0.0
3.4
34.4
2.4
1.6
11.6
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
16.2
17.5
1.3
27.4
0.4
0.2
4.8
0.0
0.0
0.0
0.0
0.6
0.0
3.1
17.7
2.2
7.4
39.1
0.2
0.2
7.4
0.2
0.2
0.0
0.0
1.4
0.0
7.0
26.7
EP T
ED
0.0
12.6
1.2 0.0
34.4
0.0
1170
0.0
9.3
6.3
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
11
1170.5
7.2
55.0
5.2
17.4
0.8
0.8
0.0
0.4
0.0
0.0
0.2
0.0
0.0
0.0
4.0
10
1180.7
2.6
28.0
1.7
7.1
0.0
0.2
1.7
0.0
0.2
0.0
0.0
3.5
0.0
3.7
16.8
9
1182.5
3.4
43.7
0.0
33.6
0.0
0.6
1.6
0.0
1.4
0.0
0.4
0.2
0.0
2.2
8.9
8
AC C
24
0.0
11.4
MA
9-11-37-17W4
0.0
SC
8
0.6
PT
1558.4
RI
12
1183.1
22.0
15.4
0.2
17.4
1.0
1.4
2.4
0.0
2.2
0.0
0.0
0.0
0.0
4.6
28.4
7
1183.8
1.2
69.7
0.8
14.5
0.4
0.0
1.6
0.0
0.0
0.0
0.0
0.0
0.0
1.0
5.0
6
1190.7
16.8
10.2
0.2
27.3
1.2
0.6
5.2
0.0
1.1
0.0
0.0
1.0
0.2
2.2
22.8
5
1199.8
0.0
0.0
0.0
0.0
0.0
0.0
2.6
0.0
0.0
0.0
23.7
5.4
0.0
0.0
0.0
4
1200
0.8
25.2
3.4
43.6
1.0
3.4
2.4
0.2
0.4
0.0
0.8
0.2
0.6
0.0
4.2
3
1200.5
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
2
1207.45
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
1
1207.6
0.0
3.8
2.6
0.4
0.0
0.0
1.8
0.0
0.0
0.0
0.4
4.2
0.0
0.0
1.2
0.8
30.8
0.0
55.6
0.6
0.6
3.1
0.2
0.0
0.0
0.0
0.0
0.0
2.8
4.1
12
14-29-45-23W5 25
1254
ACCEPTED MANUSCRIPT 19.1
13.9
0.0
23.3
0.0
0.2
4.0
0.0
0.4
0.0
0.0
0.0
0.0
4.6
23bis
1254.5
47.5
15.3
0.0
24.7
0.0
0.0
3.7
0.4
4.2
0.0
0.0
0.0
0.0
0.0
1.0
23
1254.75
17.8
13.1
0.0
39.9
0.0
0.4
3.1
0.0
1.4
0.0
0.0
0.0
0.0
3.5
17.2
22
1254.85
6.7
58.1
0.8
20.7
0.0
0.0
1.3
0.6
2.1
0.0
0.0
0.0
0.0
0.0
21
1255.3
0.8
43.9
1.2
3.8
0.0
0.0
10.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.6
20
1256.3
3.8
2.8
1.6
1.4
0.0
0.0
4.6
0.0
0.0
0.0
0.0
1.0
0.8
6.4
29.1
19
1257.4
0.0
5.8
0.8
0.0
0.0
0.0
0.6
0.0
0.0
0.0
0.0
0.4
0.0
0.0
18
1258.3
4.6
49.4
0.2
27.0
0.4
0.0
2.2
1.0
0.6
0.0
0.0
0.0
0.0
0.2
3.4
17
1281.4
8.6
8.6
0.0
23.3
0.0
0.6
3.3
0.0
1.0
0.0
0.0
0.0
0.0
10.3
39.1
16
1282.4
7.0
4.4
0.0
40.1
0.0
0.0
3.2
0.6
0.2
0.0
0.0
0.0
0.0
9.9
26.0
15
1282.9
3.0
18.2
0.0
26.1
0.2
0.2
0.8
0.2
0.2
0.0
0.0
0.0
0.0
7.1
41.8
14
1283.4
13.8
47.4
0.0
25.8
0.4
0.0
1.4
0.0
1.4
0.0
0.0
0.0
0.2
2.0
5.0
13
1283.7
4.3
5.7
0.0
42.6
0.0
0.0
5.3
0.0
0.8
0.0
0.0
0.0
0.0
5.9
26.8
12
1284.3
5.0
26.1
0.0
47.3
0.2
0.0
4.4
0.0
1.0
0.0
0.0
0.0
0.0
5.0
9.8
11
1285.5
6.3
5.7
0.0
35.4
0.2
0.8
3.1
0.0
1.2
0.0
0.0
0.0
0.0
12.7
29.1
10
1285.82
0.0
6.6
0.6
0.8
0.0
0.0
0.4
0.0
0.0
0.0
0.0
0.2
0.0
0.0
2.5
9
1289.6
0.0
3.0
1.0
0.2
0.0
0.0
7
1292.5
3.1
24.8
0.6
22.0
0.4
0.2
6
1321
0.0
0.2
0.4
14.3
0.0
1.2
SC
RI
PT
1254.2
29.1
3.8
0.4
0.0
0.0
0.2
0.6
0.0
0.2
2.0
10.6
0.2
0.2
0.0
1.0
0.8
0.4
3.1
15.5
7.6
0.0
0.0
0.0
0.0
1.0
0.0
2.2
29.9
NU
24
1321.35
6.9
8.1
0.0
41.0
0.6
0.6
1.6
0.2
1.4
0.2
0.0
0.0
0.0
5.7
25.6
1321.45
7.7
6.5
0.0
53.1
0.2
0.4
3.2
0.0
1.4
0.0
0.0
0.0
0.0
6.9
15.6
4
1321.5
3.8
14.9
0.2
41.0
0.2
1.0
1.6
0.2
0.6
0.0
0.0
0.2
0.0
4.8
25.9
3
1322
0.4
1.2
0.0
30.7
0.0
0.8
0.6
0.0
0.8
0.0
0.0
0.0
0.4
21.9
35.6
2
1322.5
7.1
1.0
0.0
32.3
0.4
1.3
2.5
0.2
1.7
0.0
0.0
0.0
0.4
5.4
32.1
1
1323.05
0.2
4.8
3.6
0.6
0.0
0.0
2.4
0.2
0.2
0.0
0.8
1.0
0.2
0.0
0.2
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.2
0.0
0.6
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
1323
0.0
44.0
15
1323.8
1.6
39.9
14
1325.4
0.0
2.0
13
1325.9
0.0
12
1326.1
1.0
11
1326.3
10 9 8
1327.5
0.0
12.6
7
1332.1
0.6
51.1
6
1332.3
0.4
5
1332.5
4
1335.5
3
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
23.3
0.8
0.6
3.8
0.4
0.0
0.0
0.0
0.0
0.0
4.2
25.2
21.1
34.8
0.0
19.8
0.2
0.0
1.5
0.0
3.8
0.0
0.0
0.2
0.0
2.1
13.2
1326.5
9.6
18.2
0.4
19.0
0.0
1.2
4.2
0.4
1.4
0.0
0.0
0.0
0.0
2.8
34.2
1327
10.5
22.5
0.0
22.1
0.2
0.8
5.7
0.0
1.6
0.0
0.0
0.0
0.0
2.6
17.8
0.8
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
1.2
31.5
0.8
0.2
1.6
0.0
0.2
0.0
0.0
0.2
0.0
0.2
1.8
33.7
7.8
0.6
0.0
0.0
2.6
0.0
0.0
0.0
0.0
0.6
0.0
0.2
2.0
4.2
49.2
3.1
2.2
1.6
0.2
4.7
0.0
0.9
0.0
0.5
0.7
0.9
0.0
0.7
0.6
14.5
6.7
1.8
0.0
0.0
3.8
0.0
0.0
0.0
0.0
2.4
0.0
0.6
6.3
1336.1
0.4
3.7
1.3
1.2
0.2
0.0
0.0
0.0
0.0
0.0
0.0
0.2
0.0
0.0
0.8
2
1339.8
0.0
4.2
7.0
0.0
0.0
0.0
1.0
0.0
0.0
0.0
0.0
6.0
0.0
0.0
2.8
1
1340.1
0.0
18.2
20.5
0.6
0.0
0.0
7.6
0.0
0.0
0.0
0.0
3.4
0.0
0.0
0.0
EP T
0.0
32.3
AC C
16
ED
10-36-39-22W4
MA
5 4b
06-07-40-20W4 12
1560.5
0.0
0.2
0.8
0.0
0.0
0.6
18.6
0.0
0.2
0.0
0.0
9.0
0.0
1.6
0.4
11
1561
0.0
0.0
2.2
0.0
0.0
0.8
20.8
0.0
0.8
0.0
0.0
7.0
0.0
0.0
0.4
10
1561.6
0.0
0.0
4.5
0.0
0.0
0.4
22.3
0.0
0.2
0.0
0.0
3.7
0.0
0.0
1.0
9
1562.1
0.0
0.0
4.2
0.0
0.0
0.1
4.5
0.0
0.2
0.0
0.0
4.0
0.0
0.0
0.6
8
1562.8
0.0
0.2
14.2
0.4
0.0
0.4
22.4
0.0
0.0
0.0
0.0
1.4
0.0
0.2
0.8
ACCEPTED MANUSCRIPT 7
1563.5
0.0
0.0
15.0
0.0
0.0
0.1
1.0
0.0
0.0
0.0
0.0
0.2
0.0
0.0
6
1564.1
0.0
0.0
4.4
0.0
0.0
5
1567.2
0.0
1.2
1.2
3.6
0.0
4
1564.1
0.0
0.8
1.6
0.0
3
1580.6
1.4
35.6
2.8
39.0
2
1581
0.0
2.6
0.4
1
1581.5
0.0
0.7
0.8
0.0
0.5
0.0
0.0
0.0
0.0
1.2
0.0
0.0
0.2
0.0
11.2
0.0
0.0
0.2
0.0
1.8
0.0
1.0
15.8
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.2
0.0
0.0
3.4
0.4
0.2
0.0
0.0
0.2
0.0
0.0
2.8
13.4
0.0
0.0
4.6
1.6
0.0
0.0
1.6
0.2
0.0
1.0
25.0
5.6
0.0
0.0
0.0
9.7
0.0
0.0
0.0
0.0
0.6
0.0
0.0
0.0
8-13-44-2W5 1788.85
0.0
63.5
0.0
13.7
0.0
0.2
0.6
0.0
0.0
0.0
0.0
0.6
0.0
4.6
6.8
6
1791
0.8
8.9
1.4
1.2
0.0
0.2
5.8
0.0
0.0
0.0
2.4
3.2
0.0
0.0
14.7
5
1794.6
0.0
19.7
5.1
11.3
0.0
0.8
1.4
0.0
0.0
0.0
3.4
0.2
0.0
2.2
17.4
4
1798.3
2.3
34.8
3.3
7.2
0.0
0.0
0.4
0.0
0.0
0.0
0.0
0.0
0.0
0.0
0.8
3
1798.57
4.3
15.9
0.2
56.7
0.0
0.4
2.4
0.0
1.0
2
1799.1
0.2
2.2
3.2
23.5
0.0
2.2
1.2
1
1799.97
3.0
30.0
0.0
45.5
0.0
2.0
2.2
2267.7
0.0
12.1
0.4
31.1
0.0
2.0
3
2277
0.4
9.5
0.0
40.0
0.0
0.7
2
2279
0.2
4.5
0.0
23.9
0.0
1.4
1
2289.5
0.2
30.7
0.4
22.4
0.0
918.5
0.4
20.8
5.8
12.0
4
919
1.4
31.8
6.3
3
935.2
1.9
20.7
0.6
2
935.5
0.0
2.8
2.6
1
935.9
8.1
9.9
0.2
7.1
8.2
1.4
0.0
1.8
11.9
0.2
1.0
0.0
0.0
0.0
0.0
2.6
9.9
RI
2.2
0.0
0.0
0.0
0.0
0.0
0.0
0.0
12.1
34.1
0.0
0.2
0.0
0.0
0.2
0.0
2.8
16.9
1.0
0.0
0.0
0.0
0.0
0.0
0.0
7.3
31.1
0.0
0.4
0.0
0.6
0.0
0.0
0.2
0.0
0.2
3.0
0.2
1.4
7.0
0.0
7.4
0.0
0.0
1.8
0.0
2.8
7.4
2.5
0.0
0.0
0.8
0.0
0.0
0.0
0.0
0.4
0.0
0.0
0.0
38.4
0.0
0.6
1.6
0.0
0.8
0.0
0.0
0.2
0.0
9.2
19.2
1.2
0.0
0.0
5.5
0.0
3.6
0.0
0.0
0.0
0.0
5.7
34.6
29.5
0.4
0.4
4.8
0.0
3.0
0.0
0.0
0.0
0.0
5.5
26.1
MA
ED
EP T AC C
0.0
0.0
1.2
15-08-63-05W5 5
0.0
0.4
1.0
NU
4
0.0
0.0
SC
8-4-42-5W5
PT
7
ACCEPTED MANUSCRIPT Appendix 2 Vs/Vd
SF/F
IR
V/I
T/F
W/D
S/D
TPI
GI
VI
GWI
1558.4
0.3
6.1
2.4
0.8
1.1
2.9
1.0
1.0
0.9
1.0
0.0
11
1559
0.3
8.4
3.3
0.6
0.7
4.9
1.4
1.4
0.7
1.5
0.0
10
1559.2
0.1
4.1
10.4
0.4
0.5
19.0
2.1
2.0
0.5
2.0
0.0
9
1559.6
0.4
4.9
2.3
0.4
0.6
2.4
1.3
1.4
0.4
1.3
0.9
8
1560
0.3
4.7
3.4
2.2
2.8
4.3
0.6
0.7
2.2
0.6
0.0
7
1560.5
0.4
4.5
7.1
1.9
2.2
9.7
0.9
1.0
2.0
1.0
0.0
6
1571.5
5.0
-
1.3
19.3
34.7
2.4
1.6
19.3
2.0
1.7
5
1573.9
1.2
-
4.0
10.1
12.6
15.8
1.3
2.4
10.1
2.3
11.2
4
1574.2
1.5
15.0
5.3
11.5
13.7
32.7
1.6
1.6
11.5
1.6
0.0
3
1574.6
0.4
6.2
4.4
0.7
0.9
2 1
1575 1575.8
0.1 2.1
2.9 4.5
3.0 1.3
3.0 4.1
4.0 7.4
1122.2
1.7
14.0
3.2
3.8
23
1127
0.6
3.8
5.3
3.5
22
1132.1
1.3
4.2
4.6
21
1132.45
0.8
8.5
3.2
19
1146.4
0.2
-
0.1
20
1146.8
-
-
18
1146.9
1.5
3.5
17
1149.35
1.1
12.3
16
1167.4
0.1
10.1
15
1167.8
0.2
-
14 13
1168.1 1168.6
1.2 0.2
5.7 3.8
12 11
1170 1170.5
10 9
1180.7 1182.5
8 7
1183.1 1183.8
6 5 4 3
1.5
1.4
0.8
1.5
0.1
3.1 6.5
0.4 1.8
0.4 1.9
3.2 4.3
0.4 1.8
0.0 0.1
5.0
3.0
1.3
2.2
4.1
1.3
1.1
3.8
0.8
1.0
3.5
0.8
0.7
2.6
7.7
1.8
2.0
2.2
1.9
1.3
2.2
2.9
5.8
1.1
1.2
2.2
1.1
0.7
NU
4.2
2.1
12.7
0.1
0.1
-
-
-
-
-
-
-
-
-
-
-
-
0.3
0.6
2.8
0.2
0.2
-
-
-
-
2.2
2.4
3.5
4.1
1.2
1.4
2.6
1.2
0.6
18.9
0.9
0.9
20.0
1.1
1.2
0.9
1.2
1.6
5.7
0.4
0.5
6.8
2.0
-
-
-
-
6.7 5.0
2.6 1.2
3.0 1.5
7.5 3.2
1.5 0.8
1.8 0.9
2.7 1.3
1.5 0.8
0.6 0.8
MA
1.4
-
ED
EP T
6.1
2.8
-
20.0
20.6
21.6
165.5
2.9
3.8
20.6
3.6
0.3
3.5 1.4
4.5 4.0
0.9 3.5
0.9 5.6
1.9 7.3
2.3 11.2
1.7 1.5
1.8 1.6
1.0 5.7
1.6 1.5
0.5 0.4
2.1 4.6
6.2 5.0
7.5 2.5
1.5 10.3
1.7 14.4
11.4 20.2
3.0 4.0
3.3 4.6
1.6 10.6
3.1 4.2
0.4 0.2
1.0
10.4
2.6
1.6
2.3
3.9
1.3
1.4
1.7
1.3
0.6
1199.8
-
-
-
-
-
-
-
-
-
-
-
1200
0.6
-
5.3
15.5
18.4
7.9
0.6
0.7
16.1
0.6
0.9
AC C
24
18.7
SC
9-11-37-17W4
PT
12
RI
Well/ Depth sample (m) 10-25-40-25W4
1190.7
1200.5
-
-
-
-
-
-
-
-
-
-
-
2
1207.45
-
-
-
-
-
-
-
-
-
-
-
1
1207.6
1.3
-
-
5.7
5.7
2.3
1.0
-
-
-
-
10.9
12.8
9.0
0.6
0.7
10.9
0.6
0.0
14-29-45-23W5 25
1254
0.6
1.5
5.8
24
1254.2
1.4
6.3
13.0
1.6
1.7
10.1
2.2
2.6
1.6
2.2
0.1
23bis
1254.5
2.5
-
0.8
39.8
87.5
17.2
2.2
2.6
87.5
2.4
0.0
23
1254.75
0.8
4.9
9.4
3.1
3.4
10.1
1.1
1.2
-
1.2
-
22
1254.85
3.0
-
-
-
-
49.8
2.8
3.1
-
3.0
0.1
21
1255.3
8.9
-
-
82.8
82.8
4.5
3.0
11.9
82.8
3.3
0.8
1256.3
2.2
1.4
1.5
1.3
1.4
2.9
19
1257.4
7.3
-
-
-
18
1258.3
2.0
17.0
9.0
20.4
-
9.7
4.1
22.7
24.0
1.9
-
-
5.8
15.9
2.1
21.5
1.9
0.1
17
1281.4
0.7
3.8
11.8
0.8
0.8
9.4
2.2
2.4
0.8
2.2
0.0
16
1282.4
0.3
2.6
4.3
1.2
15
1282.9
0.8
5.9
22.2
0.9
1.4
4.2
1.0
25.0
0.9
1.0
1.2
0.9
0.0
2.4
2.5
0.9
2.4
0.0
14
1283.4
2.4
2.5
11.7
11.5
12.5
34.1
2.5
2.6
11.5
2.5
0.0
13
1283.7
0.2
4.5
12
1284.3
0.7
2.0
4.0
1.3
12.3
4.9
1.6
3.2
0.8
0.8
1.3
0.8
0.0
5.3
8.2
0.9
0.9
4.9
0.9
0.0
11
1285.5
0.3
2.3
10
1285.82
4.7
-
7.6
1.0
-
3.2
1.2
6.3
1.2
1.3
1.0
1.3
0.0
3.2
22.8
5.1
11.4
3.2
6.5
12.0
9
1289.6
2.5
10.0
2.2
1.3
1.9
1.0
0.8
4.3
1.3
0.8
27.4
7
1292.5
6
1321
1.2
5.0
0.0
13.6
2.5
2.0
2.7
2.6
1.1
1.6
2.1
1.1
0.2
0.7
0.2
0.5
0.7
0.5
0.6
0.2
0.5
0.1
5
1321.35
0.4
4.5
4.1
1.5
1.8
5.4
0.9
1.0
1.5
1.0
0.0
4b
1321.45
4
1321.5
0.3
2.3
4.5
2.5
3.0
0.5
5.4
5.5
1.7
3
1322
0.1
1.6
7.8
0.5
2
1322.5
0.3
5.9
2.5
1
1323.05
1.2
-
1.0
-
10-36-39-22W4
0.2
0.3
1.6
4.5
0.6
2.5
0.6
0.0
2.0
9.9
0.6 1.1
1.1
1.8
1.1
0.0
0.6
13.1
1.7
1.6
0.6
1.7
0.0
0.8
1.1
3.4
1.0
1.0
0.9
1.0
0.1
23.0
46.0
1.5
0.7
6.5
23.0
1.0
15.3
NU
4.5
SC
20
RI
0.2
PT
ACCEPTED MANUSCRIPT
1323
-
-
15
1323.8
-
-
14
1325.4
-
-
13
1325.9
-
-
-
-
-
-
-
-
-
-
-
12
1326.1
1.4
6.0
4.1
1.6
2.0
7.4
2.0
2.1
1.7
1.9
0.0
11
1326.3
2.8
6.3
38.3
4.8
5.0
47.5
3.3
3.5
5.0
3.5
0.0
10
1326.5
1.4
12.2
61.7
1.3
1.3
15.4
2.7
3.3
1.3
2.8
0.2
9
1327
1.5
6.8
1.3
1.5
2.8
2.6
1.2
1.4
1.6
1.3
0.0
8
1327.5
7
1332.1
6
1332.3
5
1332.5
4
1335.5
2 1
-
-
-
-
-
-
-
-
-
-
-
-
-
-
-
-
-
-
-
-
-
-
-
-
ED
EP T -
-
-
-
-
-
-
-
-
-
-
1.6
9.0
-
42.7
42.7
33.6
1.6
1.7
42.7
1.6
0.1
4.1
10.0
11.0
17.7
19.3
13.0
3.2
45.4
17.7
9.1
1.5
10.1
-
3.5
67.2
86.4
11.5
5.2
22.5
86.4
6.8
0.6
1.8
10.5
2.0
2.3
3.4
3.1
1.4
4.2
2.3
2.0
3.5
1336.1
1.6
-
4.0
6.8
8.5
24.5
1.8
3.5
6.8
3.1
17.4
1339.8
0.6
-
14.0
3.7
4.0
5.8
0.9
35.0
3.7
1.0
18.8
1340.1
0.9
-
0.0
13.1
-
1.7
0.6
5.1
13.1
1.2
2.5
AC C
3
-
-
MA
16
06-07-40-20W4 12
1560.5
0.3
0.3
0.0
0.0
0.8
0.1
0.0
0.0
0.0
0.0
72.0
11
1561
0.0
-
0.0
0.0
7.5
0.0
0.0
0.0
0.0
0.0
-
10
1561.6
0.0
-
0.0
0.1
5.0
0.1
0.0
0.0
0.1
0.0
-
9
1562.1
0.0
-
0.0
0.1
7.7
0.1
0.0
0.0
0.1
0.0
-
8
1562.8
0.0
4.0
0.1
0.8
14.8
0.8
0.0
0.1
0.8
0.1
312.0
7
1563.5
0.0
-
0.1
1.2
18.8
1.3
0.0
0.1
1.2
0.1
-
6
1564.1
0.0
-
0.1
1.3
22.0
1.4
0.0
0.1
1.3
0.0
-
5
1567.2
0.3
15.8
0.3
0.1
0.4
0.4
0.3
0.3
0.1
0.3
16.2
4
1564.1
0.5
-
-
12.0
12.0
-
0.6
-
12.0
-
121.8
3
1580.6
0.9
-
3.5
21.9
28.1
37.2
0.9
1.0
23.2
0.9
1.4
ACCEPTED MANUSCRIPT 2
1581
0.2
25.0
1.0
0.3
0.6
1.8
0.7
0.7
0.4
0.7
14.6
1
1581.5
0.1
-
0.0
0.8
-
0.7
0.0
0.1
0.8
0.0
108.4
4.6
1.5
1.5
4.1
6.8
12.9
3.8
3.5
4.8
3.7
0.0
6
1791
3.7
-
14.7
0.8
0.9
2.7
2.1
11.1
0.8
1.8
5.6
5
1794.6
1.2
7.9
6.5
1.6
1.9
6.0
1.7
2.7
1.8
2.2
1.2
4
1798.3
3.5
-
0.1
7.7
59.5
6.5
2.3
3.0
7.7
2.9
1.0
3
1798.57
0.4
1.2
25.5
4.9
5.1
11.8
0.6
0.6
4.9
0.6
0.0
2
1799.1
0.1
6.6
0.3
0.6
2.3
0.4
0.2
0.3
0.6
0.3
0.6
1
1799.97
0.7
3.8
4.2
5.2
6.4
9.5
0.9
0.9
5.4
0.9
0.0
1.5
0.9
1.5
0.1
0.6
0.6
2.0
0.6
0.4
PT
1788.85
1.5
1.7
0.9
0.9
0.5
0.9
0.2
21.3
1.4
1.4
12.3
1.4
0.8
SC
7
RI
8-13-44-2W5
8-4-42-5W5 4
2267.7
0.4
2.8
6.8
0.9
1.0
8.1
3
2277
0.2
6.0
2.4
1.8
2.6
3.7
2
2279
0.2
4.3
1.5
0.5
0.8
1
2289.5
1.4
15.0
2.3
11.7
16.8
15-08-63-05W5 5
918.5
1.2
2.6
0.5
1.3
4
919
3.8
-
-
-
3
935.2
0.6
2.1
4.2
1.8
2
935.5
0.7
6.1
1.2
1
935.9
0.6
4.7
2.7
1.2
0.7
1.0
1.4
1.0
0.4
-
42.3
3.4
13.0
-
8.9
1.6
6.5
1.1
1.1
1.8
1.1
0.0
0.2
1.1
1.0
1.2
0.1
1.2
2.5
1.1
1.5
3.4
1.1
1.2
1.2
1.2
0.0
NU
2.2
0.1
MA ED EP T AC C
4.0
ACCEPTED MANUSCRIPT
Depth (m)
M oist (%)
Ash (%)
Volatil M atter (%)
C (%)
H (%)
N (%)
S (%)
12
1558.4
3.13
1.71
29.13
83.38
4.64
1.34
0.42
11
1559
3.14
2.35
29.24
79.18
4.47
1.27
0.38
10
1559.2
2.04
67.82
11.59
21.43
1.71
0.45
0.27
9
1559.6
2.36
32.66
20.32
52.85
3.28
0.75
0.28
8
1560
2.99
4.28
34.20
78.36
5.01
1.66
0.65
7
1560.5
2.36
13.49
36.23
68.17
4.25
1.17
6
1571.5
2.29
58.16
19.24
28.96
2.48
0.69
4.18
5
1573.9
2.13
39.11
29.76
45.93
3.36
0.98
9.36
4
1574.2
2.85
7.85
37.48
73.97
PT
0.45
5.04
1.60
0.54
3
1574.6
2.73
8.31
31.27
76.34
4.67
1.36
1.52
2
1575
2.73
33.47
28.08
51.75
RI
Appendi x 3 – Elemental Analysis data Well/sample
3.89
1.08
1.20
1
1575.8
1.25
89.08
5.86
6.66
0.88
0.25
0.11
24
1122.2
4.45
50.15
20.57
35.95
2.57
0.80
0.58
23
1127
5.14
2.46
44.29
75.14
2.30
1.50
0.72
22
1132.1
3.91
42.17
20.36
33.42
2.43
0.88
0.70
21
1132.45
5.40
3.69
33.80
74.55
4.23
1.56
0.52
19
1146.4
3.72
59.98
16.96
25.91
2.11
0.68
0.29
20
1146.8
2.93
81.04
11.03
10.27
1.25
0.45
0.49
18
1146.9
3.12
73.20
15.06
14.47
1.75
0.42
0.25
17
1149.35
4.19
15.48
16
1167.4
3.84
15
1167.8
2.07
14
1168.1
4.62
13
1168.6
5.19
12
1170
2.53
11
1170.5
6.18
10
1180.7
4.72
9
1182.5
8
1183.1
59.77
3.59
1.22
9.70
22.74
37.97
2.68
0.89
1.95
56.41
33.97
26.08
1.50
0.50
0.34
25.64
29.97
54.59
3.65
1.21
1.13
2.81
36.01
75.60
4.54
1.53
0.57
86.69
8.28
6.33
0.97
0.34
0.86
10.48
32.29
67.44
4.25
1.48
0.49
33.32
22.97
50.37
3.04
0.95
0.42
5.82
1.76
38.06
75.15
4.94
1.38
0.77
5.14
3.36
37.28
74.08
4.76
1.50
0.75
1183.8
5.99
6.05
37.24
70.93
4.69
1.49
1.68
1190.7
5.38
3.86
33.44
75.58
4.37
1.33
0.45
1199.8
4.5
92.46
6.8
2.7
0.73
0.23
0.07
1200
5.12
26.92
31.9
52.36
3.78
1.15
3.56
3
1200.5
6.47
90.05
6.66
3.08
0.78
0.24
0.57
2 1
1207.45 1207.6
3.96 3.59
84.86 83.01
10.62 9.46
5.38 8.92
1.14 1.02
0.24 0.37
0.24 0.6
25
1254
2.97
7.42
39.34
72.37
5.05
1.41
5.53
7 6 5 4
EP T
ED
31.99
45.82
AC C
MA
NU
9-11-37-17W4
SC
10-25-40-25W4
14-29-45-23W5 24
1254.2
3.41
2.56
37.73
78.45
5.12
1.84
1.23
23bis
1254.5
2.64
16.83
27.41
68.94
4.07
1.24
2.03
23
1254.75
2.88
12.59
34.79
69.71
4.67
1.49
0.92
22
1254.85
3.25
16.07
35.95
62.86
4.35
1.44
8.55
21
1255.3
2.35
59.99
18.61
25.28
2.28
0.67
6.04
4.14
1.19
1.87
7.66
5.26
1.03
0.27
0.28
36.63
68.43
4.80
1.50
2.50
27.93
48.93
3.07
0.75
16.81
2.85
37.23
78.77
5.01
1.50
0.99
2.35
34.82
79.42
4.92
1.68
0.70
3.20
11.72
32.28
71.86
4.41
1.46
0.71
1283.7
2.81
4.78
35.76
77.96
4.94
1.44
0.65
1284.3
3.07
1.12
33.64
80.98
4.78
1.52
0.65
11
1285.5
2.95
1.46
37.75
80.64
5.07
1.74
0.75
10
1285.82
1.80
90.17
7.45
2.92
0.90
0.12
9
1289.6
2.30
86.77
8.20
6.37
1.09
0.16
0.08
7
1292.5
3.12
19.43
28.75
67.66
4.29
1.16
0.68
6
1321
3.00
4.98
26.01
80.38
PT
0.72
4.13
1.11
0.27
5
1321.35
3.71
2.07
2.07
81.65
4.99
1.47
0.44
4b
1321.45
3.02
2.73
2.73
80.19
RI
1256.3
3.13
21.14
19
1257.4
1.66
88.45
18
1258.3
2.82
13.93
17
1281.4
1.80
27.09
16
1282.4
3.00
15
1282.9
3.46
14
1283.4
13 12
4.99
1.45
0.55
4
1321.5
3.20
2.06
2.06
80.44
4.69
1.25
0.77
3
1322
3.21
4.84
4.84
79.69
4.68
1.31
0.33
2
1322.5
2.62
7.64
7.64
76.65
4.36
1.23
0.39
1
1323.05
3.13
88.47
7.44
5.55
0.99
0.18
0.34
16
1323
1.96
86.07
7.17
7.47
1.06
0.32
0.20
15
1323.8
2.23
83.69
8.45
8.98
1.13
0.33
0.83
14
1325.4
2.17
92.07
6.30
2.33
0.84
0.22
0.12
13
1325.9
5.10
5.97
35.65
72.79
4.63
1.46
2.62
12
1326.1
3.46
9.71
28.24
73.43
3.92
1.19
3.63
11
1326.3
4.55
2.05
35.51
79.86
5.04
1.48
0.50
10
1326.5
4.26
1.49
34.73
80.68
4.93
1.52
0.50
9
1327
3.65
1.92
34.74
80.39
4.95
1.49
0.49
8
1327.5
1.62
93.04
6.11
1.44
0.83
0.19
0.09
7
1332.1
3.92
14.62
33.49
67.67
4.53
1.57
0.93
6
1332.3
3.59
49.48
25.29
36.95
2.98
0.92
2.06
5
1332.5
3.93
20.97
29.53
59.24
3.99
1.20
4.14
4
1335.5
3.29
67.83
14.42
22.50
2.02
0.56
0.34
1336.1
3.08
89.83
7.45
3.45
0.98
0.25
0.84
1339.8
3.10
86.43
9.25
5.95
1.17
0.26
0.27
1340.1
2.89
65.97
16.47
22.61
2.08
0.63
2.32
12
1560.5
2.13
44.46
18.23
43.77
2.85
0.62
0.30
11
1561
1.88
50.14
19.10
47.94
2.98
0.71
0.32
10
1561.6
2.34
37.46
19.23
50.04
3.05
0.83
0.36
9
1562.1
2.69
35.69
20.27
51.28
3.13
0.84
0.36
8
1562.8
1.98
71.62
11.18
19.73
1.71
0.51
0.23
7
1563.5
1.87
77.41
9.91
14.74
1.43
0.43
0.21
6
1564.1
1.41
89.78
6.82
4.49
0.81
0.23
0.08
5
1567.2
2.46
29.56
22.53
56.93
3.50
1.05
0.41
4
1564.1
1.76
93.54
5.00
1.71
0.68
0.16
0.10
3
1580.6
2.47
5.44
39.41
77.24
5.32
1.71
1.42
3 2 1
EP T
ED
MA
10-36-39-22W4
27.67
NU
20
SC
63.63
AC C
ACCEPTED MANUSCRIPT
06-07-40-20W4
2
1581
2.70
37.29
17.48
50.50
2.90
0.67
0.35
1
1581.5
2.41
84.38
8.64
8.96
1.09
0.25
1.00
7
1788.85
2.12
13.13
29.85
66.15
4.07
1.03
7.52
6
1791
1.84
52.45
20.96
35.20
2.76
0.68
4.71
5
1794.6
1.61
35.13
26.34
51.83
3.68
0.89
3.76
4
1798.3
1.52
31.43
29.68
44.12
3.17
0.67
16.66
3
1798.57
1.73
8.24
34.87
76.80
5.10
1.39
1.27
2
1799.1
1.05
37.63
21.30
52.47
3.29
0.72
0.76
1
1799.97
1.70
4.97
34.97
79.80
5.02
1.47
1.14
4
2267.7
1.10
7.22
31.25
79.99
4.78
1.14
2277
0.99
13.00
27.26
75.58
PT
1.86
3
4.44
1.08
0.97
2
2279
0.94
56.98
16.52
30.85
1.96
0.51
9.43
1
2289.5
0.90
36.18
26.42
51.75
RI
ACCEPTED MANUSCRIPT
3.69
1.00
1.95
5
918.5
3.37
31.70
23.65
55.75
3.36
1.05
0.51
4
919
3.01
71.83
13.76
18.23
1.69
0.52
1.78
3
935.2
3.54
21.19
26.29
63.69
3.78
1.21
0.32
2
935.5
3.67
29.49
21.94
73.09
4.59
1.50
0.39
1
935.9
3.96
5.80
32.15
78.64
4.71
1.42
0.35
8-13-44-2W5
ED
MA
NU
15-08-63-05W5
SC
8-4-42-5W5
EP T
References
Arthur, M. A., and B. B. Sageman, 1994, Marine shales: depositional mechanisms and environments of ancient deposits: Annual Review of Earth and Planetary Sciences, v.
AC C
22, p. 499-551.
ASTM-D4239-08, 2008, Annex. ASTM-D5373-08, 2008, Standard test methods for instrumental determination of carbon, hydrogen, and nitrogen in laboratory samples of coal. ASTM-D7582-10, 1981, Standard test method for proximate analysis of coal and coke by macro thermogravimetric analysis. Banerjee, I., W. Kalkreuth, and E. H. Davies, 1996, Coal seam splits and transgressive regressive coal couplets: A key to stratigraphy of high-frequency sequences: Geology, v. 24, p. 1001-1004.
ACCEPTED MANUSCRIPT Barker, C., 1974, Pyrolysis techniques for source-rock evaluation: AAPG Bulletin, v. 58, p. 2349-2361. Behar, F., V. Beaumont, and H. D. B. Penteado, 2001, Rock-Eval 6 technology: performances and developments: Oil & Gas Science and Technology, v. 56, p. 111-134. Berner, R. A., and D. E. Canfield, 1989, A new model for atmospheric oxygen over
PT
Phanerozoic time: American Journal of Science, v. 289, p. 333-361. Bohacs, K., and J. Suter, 1997, Sequence stratigraphic distribution of coaly rocks: fundamental
RI
controls and paralic examples: AAPG bulletin, v. 81, p. 1612-1639.
SC
Bordenave, M.L., 1993. Applied petroleum geochemistry. Editions OPHRYS. Bralower, T. J., and H. R. Thierstein, 1984, Low productivity and slow deep-water circulation
NU
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interpretation of rheotrophic and raised paleomires: Bulletin de la Société Géologique de France, v. 162, p. 283-298. Cant, D. J., and B. Abrahamson, 1996, Regional distribution and internal stratigraphy of the
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Lower Mannville: Bulletin of Canadian Petroleum Geology, v. 44, p. 508-529. Cohen, A. D., W. Spackman, and R. Raymond, 1987, Interpreting the characteristics of coal seams from chemical, physical and petrographic studies of peat deposits: Geological Society, London, Special Publications, v. 32, p. 107-125. Cross, T. A., 1988, Controls on coal distribution in transgressive-regressive cycles, Upper Cretaceous, Western Interior, USA. Chalmers, G. R., R. Boyd, and C. F. Diessel, 2013, Accommodation-based coal cycles and significant surface correlation of low-accommodation Lower Cretaceous coal seams,
ACCEPTED MANUSCRIPT Lloydminster heavy oil field, Alberta, Canada: Implications for coal quality distribution: AAPG bulletin, v. 97, p. 1347-1369. Davies, R., C. Diessel, J. Howell, S. Flint, and R. Boyd, 2005, Vertical and lateral variation in the petrography of the Upper Cretaceous Sunnyside coal of eastern Utah, USA— implications for the recognition of high-resolution accommodation changes in paralic
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coal seams: International Journal of Coal Geology, v. 61, p. 13-33. Deschamps, R., S. Omodeo-Salé, C. B., R. Fierens, and E. Tristan, in press, Stratigraphic
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architecture of coal and non-marine strata of the Mannville Group in the Western
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Canadian Sedimentary Basin, South Central Alberta: Part 1: IJCG. Diessel, C. F. K., 1982, An appraisal of coal facies based on maceral characteristics: Australian
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Proceeding 20th Symposium of Department Geology, University of New Castle, New
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Diessel, C. F. K., 1992, Coal-bearing depositional systems, Springer-Verlag Berlin Heidelberg Diessel, C. F. K., R. Boyd, J. Wadsworth, D. Leckie, and G. Chalmers, 2000, On balanced and
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unbalanced accommodation/peat accumulation ratios in the Cretaceous coals from Gates Formation, Western Canada, and their sequence-stratigraphic significance: International Journal of Coal Geology, v. 43, p. 143-186.
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Diessel, C. F. K., 2007, Utility of coal petrology for sequence-stratigraphic analysis: International Journal of Coal Geology, v. 70, p. 3-34. Espitalié, J., and M. Bordenave, 1993, Source rock parameters: Bordenave, v. 35, p. 237-272. Espitalie, J., G. Deroo, and F. Marquis, 1986, La pyrolyse Rock-Eval et ses applications. Troisième partie: Oil & Gas Science and Technology, v. 41, p. 73-89. Espitalie, J., G. Deroo, and F. Marquis, 1985a, La pyrolisis Rock-Eval et ses applications: Deuxième partie: Oil & Gas Science and Technology v. 40, p. 755-784. Espitalie, J., G. Deroo, and F. Marquis, 1985b, La pyrolyse Rock-Eval et ses applications: Première Partie: Oil & Gas Science and Technology v. 40, p. 563-580.
ACCEPTED MANUSCRIPT Espitalié, J., J. L. Laporte, M. Madec, F. Marquis, P. Leplat, J. Paulet, and A. Boutefeu, 1977, Méthode rapide de caractérisation des roches mètres, de leur potentiel pétrolier et de leur degré d'évolution: Oil & Gas Science and Technology, v. 32, p. 23-42. Flint, S., J. Aitken, and G. Hampson, 1995, Application of sequence stratigraphy to coal-bearing coastal plain successions: implications for the UK Coal Measures: Geological Society,
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London, Special Publications, v. 82, p. 1-16. Gastaldo, R. A., T. M. Demko, and Y. Liu, 1993, Application of sequence and genetic
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stratigraphic concepts to Carboniferous coal-bearing strata: an example from the Black
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Warrior basin, USA: Geologische Rundschau, v. 82, p. 212-226.
Harvey, R. D., and J. W. Dillon, 1985, Maceral distributions in Illinois coals and their
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paleoenvironmental implications: International Journal of Coal Geology, v. 5, p. 141165.
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Hayes, B., J. Christopher, L. Rosenthal, G. Los, B. McKercher, D. Minken, Y. Tremblay, J. Fennell, and D. Smith, 1994, Cretaceous Mannville Group of the western Canada
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sedimentary basin, Geological Atlas of the Western Canada sedimentary basin, v. 4, Canadian Society of Petroleum Geologists and Alberta Research Council, p. 317-334.
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Holz, M., W. Kalkreuth, and I. Banerjee, 2002, Sequence stratigraphy of paralic coal-bearing strata: an overview: International Journal of Coal Geology, v. 48, p. 147-179. ICCP, 1998, The new vitrinite classification (ICCP System 1994): Fuel, v. 77, p. 349-358.
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ICCP, 2001, The new inertinite classification (ICCP System 1994): Fuel, v. 80, p. 459-471. ISO-562, 1998, Hard coal and coke - Determination of volatile matter. ISO-7404-2, 2009, Methods for the Petrographic Analysis of Coals — Part 2: Methods of Preparing Coal Samples, International Organization for Standardization Geneva, Switzerland, p. 12 pp. Jackson, P. C., 1984, Paleogeography of the Lower Cretaceous Mannville group of western Canada.
ACCEPTED MANUSCRIPT Kalkreuth, W., and D. A. Leckie, 1989, Sedimentological and petrographical characteristics of Cretaceous strandplain coals: a model for coal accumulation from the North American Western Interior Seaway: International Journal of Coal Geology, v. 12, p. 381-424. Kalkreuth, W., D. Marchioni, J. Calder, M. Lamberson, R. Naylor, and J. Paul, 1991, The relationship between coal petrography and depositional environments from selected
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coal basins in Canada: International Journal of Coal Geology, v. 19, p. 21-76. Lafargue, E., F. Marquis, and D. Pillot, 1998, Rock-Eval 6 applications in hydrocarbon
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Technology, v. 53, p. 421-437.
Lamberson, M., R. Bustin, and W. Kalkreuth, 1991, Lithotype (maceral) composition and
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variation as correlated with paleo-wetland environments, Gates Formation, northeastern British Columbia, Canada: International Journal of Coal Geology, v. 18, p. 87-124.
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Langenberg, C., B. Rottenfusser, and R. Richardson, 1997, Coal and coalbed methane in the Mannville Group and its equivalents, Alberta. In: Pemberton, S.G. and James, D.P.
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(eds.). Petroleum Geology of the Cretaceous Mannville Group, Western Canada.: Canadian Society of Petroleum Geologists, v. Memoir 18, p. 475-486.
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Marchioni, D., and W. Kalkreuth, 1991, Coal facies interpretations based on lithotype and maceral variations in Lower Cretaceous (Gates Formation) coals of Western Canada: International Journal of Coal Geology, v. 18, p. 125-162.
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Moore, T., and J. Shearer, 2003, Peat/coal type and depositional environment—are they related?: International Journal of Coal Geology, v. 56, p. 233-252. Nicolas, G., B. Pradier, and F. Vannier-Petit, 1997, Reconstitution des environnements de dépôt des sédiments organiques de plaine deltaıque. Application al’étude sédimentologique du groupe Brent (Mer du Nord): Bulletin du Centre de Recherches Elf Exploration Production, v. 21, p. 249-264. Peters, K., 1986, Guidelines for evaluating petroleum source rock using programmed pyrolysis: AAPG bulletin, v. 70, p. 318-329.
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Stach, E., M.-T. Mackowsky, M. Teichmüller, G. Taylor, D. Chandra, and R. Teichmüller, 1982, Coal petrology: Gebrüder Borntraeger, Berlin, p. 535.
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Staub, J. R., 2002, Marine flooding events and coal bed sequence architecture in southern West
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Virginia: International Journal of Coal Geology, v. 49, p. 123-145. Strobl, R., 1988, The effects of sea-level fluctuations on prograding shoreline sand estuarine
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valley fill sequences in the Glauconitic member, Medicine River field and adjacent areas. In: D.P. James and D.A. Leckie (eds.). Sequences, Sedimentology: Surface and
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Subsurface. : Canadian Society of Petroleum Geologists, v. Memoir 15, p. 221-236. Styan, W. t., and R. Bustin, 1983, Petrographyof some fraser river delta peat deposits: coal
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maceral and microlithotype precursors in temperate-climate peats: International Journal of Coal Geology, v. 2, p. 321-370.
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Suárez-Ruiz, I., D. Flores, J. G. Mendonça Filho, and P. C. Hackley, 2012, Review and update of the applications of organic petrology: Part 1, geological applications: International Journal of Coal Geology, v. 99, p. 54-112.
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Sýkorová, I., W. Pickel, K. Christanis, M. Wolf, G. Taylor, and D. Flores, 2005, Classification of huminite—ICCP System 1994: International Journal of Coal Geology, v. 62, p. 85106.
Teichmüller, M. and Teichmüller, R., 1982. Fundamentals of coal petrology. Stach, E., Mackowsky, M.-Th., Teichmüller, M., Taylor, GH, Chandra, D., and Techmüller, R., Stach’s Textbook of Coal Petrology, 3rd revised and enlarged edition: Berlin, Stuttgart, Gebrüder Borntraeger: 5-86. Teichmüller, M., 1989, The genesis of coal from the viewpoint of coal petrology: International Journal of Coal Geology, v. 12, p. 1-87.
ACCEPTED MANUSCRIPT Tyson, R., 2001, Sedimentation rate, dilution, preservation and total organic carbon: some results of a modelling study: Organic Geochemistry, v. 32, p. 333-339. Wadsworth, J., R. Boyd, C. Diessel, D. Leckie, and B. A. Zaitlin, 2002, Stratigraphic style of coal and non-marine strata in a tectonically influenced intermediate accommodation setting: the Mannville Group of the Western Canadian Sedimentary Basin, south-central
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Alberta: Bulletin of Canadian Petroleum Geology, v. 50, p. 507-541. Wadsworth, J., R. Boyd, C. Diessel, and D. Leckie, 2003, Stratigraphic style of coal and non-
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marine strata in a high accommodation setting: Falher Member and Gates Formation
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(Lower Cretaceous), western Canada: Bulletin of Canadian Petroleum Geology, v. 51, p. 275-303.
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Wadsworth, J., C. Diessel, and R. Boyd, 2010, The sequence-stratigraphic significance of paralic coal and its use as an indicator of accommodation space in terrestrial sediments:
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Figures
Fig. 1 – Location of the study area and distribution of the Mannville Group deposits. The paleogeography
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at the end of the deposition of the Upper Mannville Group and the lithology distribution is indicated (Jackson 1984). The trace line of the geological transect of Fig. 2 is shown together with the location of
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the well-logs and cores analyzed in this work.
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Fig. 2 – Geological section showing the architecture and geometry of the Mannville Group (From Deschamps et al., in press). The stratigraphic record has been subdivided in the 3rd -order system tracts. The position of the core analyzed in this work is also indicated. The trace line of the section is shown in Fig. 1.
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Fig. 3 (Part a)
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Fig. 3 (Part b) Fig. 3 – Stratigraphic section of the cores analyzed. The stratigraphic record was subdivided in 4 th -order depositional sequences. In correspondence of the coal packages 5th -order deepening and shallowing cycles were also recognized. For each sample the depositional environment where coal formed is defined,
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Fig. 4 - GI-TPI facies diagram proposed by Diessel (1986) and modified by Nicolas et al., (1997), which determines the depositional environment of the peat.
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Fig. 5 – Block-diagram illustrating the spatial distribution of the coal depositional environments
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throughout the alluvial and delta plain (Modified from Nicolas et al., 1997). Variation in the subsidence rate along the sedimentary profile determine a different vertical superimposition of the depositional
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Fig. 6 – Optical microscopy, photomicrographs taken under reflected white light. Fluorescence mode in photographs (b) and (f). Width of the longitudinal dimension of the pictures: 200 μm. Terrestrial depositional environments (a-d): (a and c) Organic matter accumulation formed by very small fragments of inertinite macerals (inertodetrinite) spore and mineral matter. Sporinite is visible in fluorescence mode (b); (d) Collodetrinite binding mostly fusinite, semifusinite macerals and mineral matter. Dry Forest depositional environment (e-h): (e) Fusinite, semifusinite and liptinite. Liptinite in fluorescence mode (f) appears as exsudatinite; (g) Fusinite and semifusinite macerals; (h) Collodetrinite binding semifusinite maceral and liptinite, where cell lumens are still recognizable.
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Fig. 7 - Optical microscopy, photomicrographs taken under reflected white light. Fluorescence mode in photographs (d) and (h). Width of the longitudinal dimension of the pictures: 200 μm. Wet Forest depositional environment (a-e): Collotellinite on the top of the photogram and telinite on the bottom. In telinite cell lumens are filled with resinite; (b) Collotellinite where cell walls are not completely homogenized; (c) Collodetrinite binding fusinite, semifusinite and sporinite macerals. On the bottom right of the image a big spore is visible in fluorescence mode (d). Swamp Forest (e-h): (e) interstratified layers of vitrinite, sporinite, resinite and mineral matter. On the top right of the image large accumulation of pyrite can be observed; (f) Fusinite with cell lumens filled with mineral matter; (g) Collodetrinite binding, vitrodetrinite, cutinite, sporinite and mineral matter. Cutinite ,sporinite and exsudatinite can be observed in fluorescence mode (h).
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Fig. 8 - Optical microscopy, photomicrographs taken under reflected white light. Fluorescence mode in photographs (d) and (h). Width of the longitudinal dimension of the pictures: 200 μm. Reed Moor depositional environment (a-d): (a and c) Collodetrinite and sporinite, inertodetrinite, semifusinite and mineral matter. Sporinite is visible in fluorescence mode (d); (b) Collodetrinite binding sporinite, inertodetrinite and funginite. Limnic depositional environment (e-h): (e) Organic matter accumulation formed by vitrinite (collotellinite and vitrodetrinite), semifusinite and sporinite, interstratified with mineral matter; (f) Collodetrinite
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semifusinite and algae; (h) In fluorescence mode, algae are well recognizable as Botryococcus braunii.
Fig. 9 - Optical microscopy, photomicrographs taken under reflected white light. Fluorescence mode in photographs (b) and (h). Width of the longitudinal dimension of the pictures : 200 μm.
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Open Moor depositional environments, formed by organic matter dispersed in mineral matter (DOM): (a, c and d) Layers of organic matter, formed by vitrinite, semifusinite, inertodetrinite and sporinite, interstratified with mineral matter. Sporinite is visible in fluorescence mode (b); (e, f and g) Fragments of organic matter, with different composition, size and preservation state, transported and deposited together with abundant mineral matter. Sporinite can be also accumulated in these deposits (h); In (e) on the right, large accumulation of pyrite and in (f) carbonate clasts deposited with organic matter fragments.
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Fig. 10 - Frequency of the occurrence of the coal depositional environments in the 4th-order system
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S ample
Depht
Lithofacies
10-25-40-25W4
12
1558.4
Coal
HST
HST
Sh
Terrestrial / Dry Forest
11
1559
Coal
HST
HST
Sh
Terrestrial
10
1559.2
Coal
HST
HST
Sh
Terrestrial
9
1559.6
Coal
HST
HST
Sh
Terrestrial
8
1560
Coal
HST
HST
Sh
Reed M oor
7
1560.5
Coal
HST
HST
Sh
Reed M oor
6
1571.5
DOM
TST
TST
Dp
5
1573.9
DOM
TST
TST
Dp
4
1574.2
Coal
TST
TST
3
1574.6
Coal
TST
TST
2
1575
Coal
TST
1
1575.8
Coal
TST
23
1127
Coal
22
1132.1
Coal
21
1132.45
Coal
20
1144.8
Coal
19
1146.4
18 17
5th
Depositional Environment
Open M oor
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Open M oor
Sh
Terrestrial
TST
Sh
Reed M oor
TST
Sh
Wet Forest / Swamp Forest
HST
TST
Sh
Liminic / Reed M oor
HST
HST
Sh
Dry Forest
HST
M FS
M FS
Reed M oor
HST
M FS
M FS
Open M oor
DOM
HST
TST
Dp
Open M oor
1146.9
DOM
HST
TST
Dp
Open M oor
1149.35
Coal
HST
TST
Sh
Reed M oor
1167.4
Coal
HST
HST
Sh
Terrestrial / Dry Forest
1167.8
DOM
HST
HST
Sh
Open M oor
1168.1
Coal
HST
HST
Dp
Dry Forest / Wet Forest
13
1168.6
Coal
HST
HST
Sh
Dry Forest
12
1170
DOM
HST
M FS
M FS
Open M oor
11
1170.5
Coal
HST
TST
Dp
Swamp Forest
10
1180.7
Coal
TST
HST
Sh
Dry Forest / Terrestrial
9
1182.5
Coal
TST
HST
Sh
Swamp Forest / Limnic
8
1183.1
Coal
TST
HST
Sh
Dry Forest
7
1183.8
Coal
TST
TST
Dp
Wet Forest / Swamp Forest
6
1190.7
Coal
LST
HST
Sh
Dry Forest / Reed M oor
5
1199.8
DOM
LST
TST
M FS
Open M oor
4
1200
DOM
LST
TST
Sh
Limnic
16 15
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DOM
LST
TST
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1122.2
Coal
HST
M FS
M FS
Wet Forest / Swamp Forest
Coal
HST
HST
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25
1254 1254.2
Coal
HST
HST
Sh
Dry Forest
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Coal
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Sh
Swamp Forest
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1254.75
Coal
HST
HST
Sh
22
1254.85
Coal
HST
HST
Sh
21
1255.3
Coal
HST
HST
20
1256.3
Coal
HST
HST
19
1257.4
DOM
HST
18
1258.3
Coal
HST
17
1281.4
Coal
HST
16
1282.4
Coal
HST
15
1282.9
Coal
14
1283.4
Coal
13
1283.7
Coal
12
1284.3
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1285.5
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Open M oor
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Sh
Dry Forest
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Sh
Dry Forest / Reed M oor
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Dry Forest
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HST
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HST
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DOM
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HST
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Open M oor
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Coal
HST
HST
Sh
Dry Forest / Reed M oor
1321
Coal
HST
HST
Sh
Terrestrial
5
1321.35
Coal
HST
HST
Sh
Dry Forest / Reed M oor
4b
1321.45
Coal
HST
HST
Sh
Reed M oor
4
1321.5
Coal
HST
HST
Sh
Dry Forest / Reed M oor
3
1322
Coal
HST
HST
Sh
Terrestrial
2
1322.5
Coal
HST
HST
Sh
Dry Forest
1
1323
DOM
HST
M FS
M FS
Open M oor
16
1323
DOM
HST
HST
Sh
Open M oor
15
1323.8
DOM
HST
HST
Sh
Open M oor
14
1325.4
DOM
HST
M FS
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Open M oor
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Pyrite Coal
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1326.3
Coal
HST
TST
Sh
Wet Forest
10
1326.5
Coal
HST
TST
Sh
Dry Forest
9
1327
Coal
HST
TST
Sh
Dry Forest
8
1327.5
DOM
HST
TST
M FS
Open M oor
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1332.1
Coal
TST
TST
Sh
Swamp Forest
6
1332.3
DOM
TST
TST
Sh
5
1332.5
DOM
TST
TST
M FS
Open M oor
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1335.5
DOM
TST
TST
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Open M oor
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1336.1
DOM
TST
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1339.8
DOM
TST
1
1340.1
DOM
TST
12
1560.5
Coal
HST
11
1561
Coal
10
1561.6
Coal
9
1562.1
Coal
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1562.8
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1563.5
6
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HST
Sh
Open M oor
HST
M FS
Open M oor
HST
Sh
Terrestrial
HST
HST
Sh
Terrestrial
HST
HST
Sh
Terrestrial
HST
HST
Sh
Terrestrial
DOM
HST
HST
Sh
Open M oor
DOM
HST
HST
Sh
Open M oor
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DOM
HST
HST
Sh
Open M oor
1567.2
Coal
HST
TST
Sh
Terrestrial
1567.5
DOM
HST
TST
M FS
Open M oor
1580.6
Coal
TST
HST
Sh
Limnic
2
1581
Coal
TST
HST
Sh
Terrestrial
1
1581.5
DOM
TST
M FS
M FS
Open M oor
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1788.85
Coal
HST
TST
Dp
Wet Forest
6
1791
DOM
HST
TST
Dp
Open M oor
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1794.6
Coal
HST
TST
Sh
Dry Forest
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1798.3
Coal
HST
TST
M FS
Swamp Forest
3
1798.57
Coal
HST
TST
Dp
Limnic
2
1799.1
Coal
HST
TST
Sh
Terrestrial
1
1799.97
Coal
HST
TST
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HST
TST
Sh
Terrestrial
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2289.5
Coal
HST
M FS
M FS
Limnic
5
918.5
Coal
HST
HST
Sh
Swamp Forest
4
919
DOM
HST
TST
M FS
Open M oor
3
935.2
Coal
HST
HST
Sh
Wet Forest
2
935.5
Coal
HST
HST
Sh
1
935.9
Coal
HST
HST
Sh
Terrestrial
Swamp Forest / Limnic
RI
15-08-63-05W5
4
PT
8-4-42-5W5
SC
Table 1 – List of the samples analyzed. For each sample it is indicated the 3rd and 4th -order depositional sequences system tracts and 5th -order eustatic sequence cycles where the relative
NU
coal layer formed, which was determined by means of facies analysis and sequential stratigraphic correlations (Fig. 2). The maximum flooding surface (MFS) indicates the
MA
maximum transgressive event. For each sample the depositional environment, defined
AC C
EP T
ED
interpreting the TPI and GI petrographical indices (Fig. 5 and Table 3), is also reported.
ACCEPTED MANUSCRIPT
Wells
10-25-4025W4 27 5.5
9-11-3717W4 95 19.5
14-29-4523W5 70.8 7.95
10-36-3922W4 26 7.5
06-07-4020W4 18.4 5.6
8-13-442W5 30.2 1.8
8-4-425W5 22.8 0.8
15-08-6305W5 36.2 1.4
Average
ST Thickness (m)
8
27.5
25
4.4
10.7
9.1
2.8
24.8
14.04
Coal cumulative Thickness (m)
3
6
8
0.4
3.7
0
0.4
1.4
2.86
Proportion in respect to the Total Coal thickness (%)
54.5
30.8
100
5.3
66.1
0
50
100
50.84
Proportion in respect to the ST thickness (%)
34.6
0
14.3
5.6
19.36
0
0.2
0.35
1.05
12.7 1.8
1.1 0.4
8.1 0
16.51 3.25
Total stratigraphic thickness (m) Total Coal thickness (m) HST
TST
LST
37.5
21.8
32
9.1
M ean coal layer Thickness (m)
3
1.2
1
0.4
ST Thickness (m) Coal cumulative Thickness (m)
15.5 2.5
61.5 13.5
8.3 0
18.6 7.1
Proportion in respect to the Total Coal thickness (%)
45.5
69.2
0
Proportion in respect to the ST thickness (%)
16.1
22
M ean coal layer Thickness (m)
2.5
2.3
ST Thickness (m)
3.5
6
Coal Thickness (m)
0
Proportion in respect to the Total Coal thickness (%)
0 0
M ean coal layer Thickness (m)
E C
U N
6.3 0.7
94.7
12.5
100
50
0
46.49
38.2
11.1
14.2
36.4
0
17.25
2.4
0.4
0.3
0.2
0
1.13
38
3
1.4
8.4
18.9
3.3
10.31
0
0
1.2
0
0
0
0.15
0
0
0
21.4
0
0
0
2.68
0
0
0
85.7
0
0
0
10.71
D E
T P
Proportion in respect to the ST thickness (%)
I R
C S 1.2
T P
0
A M 0 1
1.2
Table 2 – Thickness of the coal layers in the 4th -order depositional sequences system tracts calculated for each core analyzed
C A
40.80 6.26
1.2
ACCEPTED MANUSCRIPT
Index
Macerals Rate
Variable
Vs/Vd
Telinite+Collotellinite/Collodetri nite+Vitrodetrinite
Environmental information
Structured versus detrital organic
Vegetation Type and Degradation process
matter Semifusinite/Fusinite
Degree of oxydation in the peat
Dryness and exsposition rate
V/I
Vitrinite/Inertinite
Rate of humidity in the peat
High/Low water table
T/F
Total Vitrinite/Fusinite+Semifusinite
Rate of Gelified/Fusinized of the
Wet Forest/Dry Forest
organic matter
TPI
GI
RI
vegetation
Forest-moor versus reed-more vegetation
Degradation/Transportation processes Type of vegetation
Type of vegetation and degradation processes
Forest versus marsh vegetation
Type of vegetation
Rate of Gelified/Fusinized of the
Wet/Dry conditions
organic matter
Telinite+Collotellinite+Fusinite+ Forest versus marsh vegetation Semifusinite+Suberinite+Resinit e/ Collodetrinite+Inertinite+Sporini te
Type of vegetation
EP T
ED
VI
Forest-moor versus reed-more
SC
S/D
Structured/detrital inertinite
NU
W/D
Semifusinite+Fusinite/Inertodetri nite+M acrinite+M icrinite Telinite+Collotellinite+Fusinite+ Semifusinite / Alginite+Sporinite+Inertidetrinit e Telinite+Collotellinite+Fusinite+ Semifusinite / Alginite+Sporinite+Inertodetrinit e+Collodetrinite+Vitrodetrinite Telinite+Collotellinite+Fusinite+ Semifusinite / Collodetrinite+M acrinite+Inertod etrinite) Total Vitrinite+M acrinite/Semifusinite +Fusinite+Inertodetrinite
MA
IR
PT
SF/F
Table 3 – Petrographic indices calculated in this work and information provided by their use
AC C
(From Calder et al., 1991; Diessel, 1986; Kalkreuth and Leckie, 1989).
ACCEPTED MANUSCRIPT HST
M FS
39
8
29.29
40.33
65.33
C (%, Dry bases)
56.05
45.18
24.46
STot (%, Dry bases)
1.28
2.53
0.73
Vitrinite (%)
42.7
45.5
27.8
52.5
66
71.3
32.6
17
6.5
40
24.6
16.7
6.1
6.4
4.7
7.5
9.3
12.1
18.6
31.1
61
Mineral Matter Free-basis (%) Inertinite (%) Mineral Matter Free-basis (%) Liptinite (%) Mineral Matter Free-basis (%) M ineral M atter (%)
PT
59
Ash (%)
RI
N. samples
TST
Table 4 - Average of the most relevant petrographic and geochemical data for each 4th -order
Dry Forest
19
20
58.66 29.24
C (%)
58.51
S (%)
1.15
Wet Forest
Swamp Forest
Reed M oor
Limnic
Open M oor
7
10
7
8
35
70.56 12.30
51.77 34.52
69.66 13.67
68.69 12.31
69.84 10.99
21.24 70.57
69.55
49.79
67.54
69.77
71.57
19.36
1.83
2.39
2.90
2.01
1.49
1.43
ED
TOC (%) Ash (%)
NU
Terrestrial
MA
Number of samples
SC
depositional sequence system tract
HI (mgHC/gTOC)
150.16
159.80
145.00
185.50
178.71
237.00
150.77
OI (mgCO2/gTOC)
13.60
18.71
17.76
15.93
18.57
15.89
14.62
Vitrinite (%)
21.79
67.17
73.39
62.79
75.43
21.88
54.00 38.12
76.55 15.50
81.22 12.20
65.99 27.77
82.70 11.03
65.42 5.39
65.76 9.36
40.43 5.26
17.67 5.07
13.50 4.77
29.19 4.59
12.09 4.75
16.12 6.01
M ineral M atter (%)
10.29 9.00
5.57 5.73
5.78 12.26
5.28 9.64
4.82 4.86
5.21 8.80
17.97 66.55
Vs/Vd SF/F
0.31 7.53
1.05 5.70
3.64 5.56
1.95 7.85
0.47 5.88
0.71 4.54
-
3.31
8.91
8.48
5.96
3.68
8.01
-
0.39 1.70
1.43 1.81
15.97 17.66
16.22 27.30
2.29 3.00
9.81 12.14
-
W/D S/D
4.44 0.87
7.34 1.58
14.46 2.64
32.94 1.83
5.02 0.79
13.59 0.83
-
TPI GI
0.91 0.42
1.80 1.50
4.12 16.20
2.11 21.13
0.83 2.37
0.91 10.14
-
VI
0.89
1.62
2.71
2.02
0.79
0.86
-
EP T
50.91
23.95 59.84
Min.Matt. Free-basis (%) Inertinite (%) Min.Matt. Free-basis (%)
IR V/I T/F
AC C
Liptinite (%) Min.Matt. Free-basis (%)
Table 5 - Average of the most relevant geochemical and petrographical data of each coal depositional environment.
AC C
EP T
ED
MA
NU
SC
RI
PT
ACCEPTED MANUSCRIPT
ACCEPTED MANUSCRIPT Appendix 1 – Maceral analysis data Appendix 2 – Petrographic indices calculated on the samples containing more than 50% of organic matter (coal)
AC C
EP T
ED
MA
NU
SC
RI
PT
Appendix 3 – Elemental Analysis data