Occurrence, Classiﬁcation and Formation Mechanisms of the Organic-Rich Clasts in the Upper Paleozoic Coal-Bearing Tight Sandstone, Northeastern Margin of the Ordos Basin, China

: The detailed characteristics and formation mechanisms of organic-rich clasts (ORCs) in the Upper Paleozoic tight sandstone in the northeastern margin of the Ordos Basin were analyzed through 818-m-long drilling cores and logging data from 28 wells. In general, compared with soft-sediment clasts documented in other sedimentary environments, organic-rich clasts in coal-bearing tight sandstone have not been adequately investigated in the literature. ORCs are widely developed in various sedimentary environments of coal-bearing sandstone, including ﬂuvial channels, crevasse splays, tidal channels, sand ﬂats, and subaqueous debris ﬂow deposits. In addition to being controlled by the water ﬂow energy and transportation processes, the fragmentation degree and morphology of ORCs are also related to their content of higher plants organic matter. The change in water ﬂow energy during transportation makes the ORCs show obvious mechanical depositional di ﬀ erentiation. Four main types of ORC can be recognized in the deposits: diamictic organic-rich clasts, ﬂoating organic-rich clasts, loaded lamellar organic-rich clasts, and thin interlayer organic-rich clasts. The relationship between energy variation and ORCs deposition continuity is rarely studied so far. Based on the di ﬀ erent handling processes under the control of water ﬂow energy changes, we propose two ORCs formation mechanisms: the long-term altering of continuous water ﬂow and the short-term water ﬂow acting triggered by sudden events. in the coal-bearing sandstone strata in the northeastern margin of the Ordos Basin.


Methodology
A total of 28 exploration wells were selected as research objects in this study, drilled from 2013 to 2017 by the China United Coalbed Methane Corporation. In total, more than 818-m-long conventional cores were received from 28 wells, diffusely covering the developed intervals of the tight sandstone gas reservoirs in coal-bearing formation; additionally, all the wells were logged with a set of comprehensive wireline surveys and cuttings. The cores have been macroscopically examined and described at 1-cm scale to obtain information on lithology, sedimentary structures, and geometric features of the organic-rich clasts. Samples have been collected from the shallow marine shelf, barrier coast and fluvial-delta deposits in all the three coal-bearing formations, thus providing sufficient geological information to undertake a comprehensive study of ORCs.  Lithochronostratigraphical column of the Upper Paleozoic strata in the study area. Here, we described the development characteristics of organic-rich clasts in coal-bearing sandstones in detail through core observation, and the descriptions contain lithology, morphology, distribution, and deformation. Thirty-six typical hand specimens were selected from the cores to prepare thin sections; meanwhile, the microscopic feature information of ORC was captured by the ZEISS optical microscope. Twelve whole-rock polished blocks were prepared to carry out maceral analysis. Maceral analysis was performed under a Zeiss Axio imager microscope equipped with an oil immersion objective and a white incident and a blue light source where >800 points were considered for each sample. Maceral was classified by the ICCP (International Committee for Coal Petrology) System 1994 [63][64][65]. The lithofacies codes are named according to [66]; some codes are added and modified following [67]. Based on the facies data derived from core descriptions and logging interpretations, a series of detailed comparative analysis was made on the organic-rich clasts, in order to find out the origins and control factors of ORCs developed in different sedimentary environments.

Results
Eleven types of lithofacies related to organic-rich clasts are recognized within the Carboniferous-Permian coal-bearing strata (Table 1). These have been divided into 5 types of facies associations standing for different sedimentary processes and settings, which have been identified in cores in conjunction with the interpretation of logging curves. These facies associations are mainly interpreted as channels (fluvial channels and delta distributary channels), crevasse splays, sand flats, tidal channels, and subaqueous debris flow deposits. The occurrence of organic-rich clasts will be described in detail below, representing the variation of water-flow energy during sediment transport.
The organic-rich clasts are widely distributed in the coal-bearing tight sandstones of Benxi Formation, Taiyuan Formation and Shanxi Formation in the study area. The lithology of ORCs identified in the core includes carbonaceous clasts, carbonaceous mudstone clasts, dark mudstone clasts, shale clasts, and plant fragments ( Figure 3A-D). In terms of color, the organic-rich clasts are mostly black or grayish black, and easy to dye the hosting sandstone. Moreover, the associated pyrite, commonly identified in the core hand specimens, is a characteristic mineral formed from organic-rich Lithochronostratigraphical column of the Upper Paleozoic strata in the study area. Here, we described the development characteristics of organic-rich clasts in coal-bearing sandstones in detail through core observation, and the descriptions contain lithology, morphology, distribution, and deformation. Thirty-six typical hand specimens were selected from the cores to prepare thin sections; meanwhile, the microscopic feature information of ORC was captured by the ZEISS optical microscope. Twelve whole-rock polished blocks were prepared to carry out maceral analysis. Maceral analysis was performed under a Zeiss Axio imager microscope equipped with an oil immersion objective and a white incident and a blue light source where >800 points were considered for each sample. Maceral was classified by the ICCP (International Committee for Coal Petrology) System 1994 [63][64][65]. The lithofacies codes are named according to [66]; some codes are added and modified following [67]. Based on the facies data derived from core descriptions and logging interpretations, a series of detailed comparative analysis was made on the organic-rich clasts, in order to find out the origins and control factors of ORCs developed in different sedimentary environments.

Methodology
A total of 28 exploration wells were selected as research objects in this study, drilled from 2013 to 2017 by the China United Coalbed Methane Corporation. In total, more than 818-m-long conventional cores were received from 28 wells, diffusely covering the developed intervals of the tight sandstone gas reservoirs in coal-bearing formation; additionally, all the wells were logged with a set of comprehensive wireline surveys and cuttings. The cores have been macroscopically examined and described at 1-cm scale to obtain information on lithology, sedimentary structures, and geometric features of the organic-rich clasts. Samples have been collected from the shallow marine shelf, barrier coast and fluvial-delta deposits in all the three coal-bearing formations, thus providing sufficient geological information to undertake a comprehensive study of ORCs.

Results
Eleven types of lithofacies related to organic-rich clasts are recognized within the Carboniferous-Permian coal-bearing strata (Table 1). These have been divided into 5 types of facies associations standing for different sedimentary processes and settings, which have been identified in cores in conjunction with the interpretation of logging curves. These facies associations are mainly interpreted as channels (fluvial channels and delta distributary channels), crevasse splays, sand flats, tidal channels, and subaqueous debris flow deposits. The occurrence of organic-rich clasts will be described in detail below, representing the variation of water-flow energy during sediment transport. clasts in a local reducing microenvironment during diagenesis ( Figure 3E). The shapes of ORCs are varied, including blades, discs, plate strips, tearing chips and irregular forms. The grain size is generally gravel size, with a maximum of more than 10 cm. Although strongly deformed, the long axes of most ORCs are parallel or sub-parallel to the stratum ( Figure 3A,B). clasts in a local reducing microenvironment during diagenesis ( Figure 3E). The shapes of ORCs are varied, including blades, discs, plate strips, tearing chips and irregular forms. The grain size is generally gravel size, with a maximum of more than 10 cm. Although strongly deformed, the long axes of most ORCs are parallel or sub-parallel to the stratum ( Figure 3A,B). clasts in a local reducing microenvironment during diagenesis ( Figure 3E). The shapes of ORCs are varied, including blades, discs, plate strips, tearing chips and irregular forms. The grain size is generally gravel size, with a maximum of more than 10 cm. Although strongly deformed, the long axes of most ORCs are parallel or sub-parallel to the stratum ( Figure 3A,B). clasts in a local reducing microenvironment during diagenesis ( Figure 3E). The shapes of ORCs are varied, including blades, discs, plate strips, tearing chips and irregular forms. The grain size is generally gravel size, with a maximum of more than 10 cm. Although strongly deformed, the long axes of most ORCs are parallel or sub-parallel to the stratum ( Figure 3A,B). clasts in a local reducing microenvironment during diagenesis ( Figure 3E). The shapes of ORCs are varied, including blades, discs, plate strips, tearing chips and irregular forms. The grain size is generally gravel size, with a maximum of more than 10 cm. Although strongly deformed, the long axes of most ORCs are parallel or sub-parallel to the stratum ( Figure 3A,B).  Under the microscope, ORCs with small particle size can also be observed widely, which usually show a characteristic of compressional deformation ( Figure 3F-H). The results of microscopic observation show that these ORCs are mainly composed of organic matter (OM), fine-grained sediments ( Figure 3F-N), and some authigenic inorganic minerals (such as pyrite). As for the organic macerals, there are mainly vitrinite, inertinite and liptinite ( Figure 3I-N Under the microscope, ORCs with small particle size can also be observed widely, which usually show a characteristic of compressional deformation ( Figure 3F-H). The results of microscopic observation show that these ORCs are mainly composed of organic matter (OM), fine-grained sediments ( Figure 3F-N), and some authigenic inorganic minerals (such as pyrite). As for the organic macerals, there are mainly vitrinite, inertinite and liptinite ( Figure 3I-N Under the microscope, ORCs with small particle size can also be observed widely, which usually show a characteristic of compressional deformation ( Figure 3F-H). The results of microscopic observation show that these ORCs are mainly composed of organic matter (OM), fine-grained sediments ( Figure 3F-N), and some authigenic inorganic minerals (such as pyrite). As for the organic macerals, there are mainly vitrinite, inertinite and liptinite ( Figure 3I-N Under the microscope, ORCs with small particle size can also be observed widely, which usually show a characteristic of compressional deformation ( Figure 3F-H). The results of microscopic observation show that these ORCs are mainly composed of organic matter (OM), fine-grained sediments ( Figure 3F-N), and some authigenic inorganic minerals (such as pyrite). As for the organic macerals, there are mainly vitrinite, inertinite and liptinite ( Figure 3I-N Under the microscope, ORCs with small particle size can also be observed widely, which usually show a characteristic of compressional deformation ( Figure 3F-H). The results of microscopic observation show that these ORCs are mainly composed of organic matter (OM), fine-grained sediments ( Figure 3F-N), and some authigenic inorganic minerals (such as pyrite). As for the organic macerals, there are mainly vitrinite, inertinite and liptinite ( Figure 3I-N Under the microscope, ORCs with small particle size can also be observed widely, which usually show a characteristic of compressional deformation ( Figure 3F-H). The results of microscopic observation show that these ORCs are mainly composed of organic matter (OM), fine-grained sediments ( Figure 3F-N), and some authigenic inorganic minerals (such as pyrite). As for the organic macerals, there are mainly vitrinite, inertinite and liptinite ( Figure 3I-N). Vitrinite (type III kerogen, The organic-rich clasts are widely distributed in the coal-bearing tight sandstones of Benxi Formation, Taiyuan Formation and Shanxi Formation in the study area. The lithology of ORCs identified in the core includes carbonaceous clasts, carbonaceous mudstone clasts, dark mudstone clasts, shale clasts, and plant fragments ( Figure 3A-D). In terms of color, the organic-rich clasts are mostly black or grayish black, and easy to dye the hosting sandstone. Moreover, the associated pyrite, commonly identified in the core hand specimens, is a characteristic mineral formed from organic-rich clasts in a local reducing microenvironment during diagenesis ( Figure 3E). The shapes of ORCs are varied, including blades, discs, plate strips, tearing chips and irregular forms. The grain size is generally gravel size, with a maximum of more than 10 cm. Although strongly deformed, the long axes of most ORCs are parallel or sub-parallel to the stratum ( Figure 3A,B).  Figure 3N) and bituminite with obvious fluorescence characteristics are seen. Thus, it can be seen that the organic matter found in ORCs is mainly derived from terrestrial higher plants.  Under the microscope, ORCs with small particle size can also be observed widely, which usually show a characteristic of compressional deformation ( Figure 3F-H). The results of microscopic observation show that these ORCs are mainly composed of organic matter (OM), fine-grained sediments ( Figure 3F-N), and some authigenic inorganic minerals (such as pyrite). As for the organic macerals, there are mainly vitrinite, inertinite and liptinite ( Figure 3I-N). Vitrinite (type III kerogen, formed by the gelification of plant remains) is the most abundant organic component, with light gray to gray under the reflected light ( Figure 3I-M). Most of these Vitrinite components are collotelinite ( Figure 3I,K), collodetrinite ( Figure 3J) and vitrodetrinite ( Figure 3I,K-M). Vitrodetrinite, especially for the muddy ORCs, is present in the form of small discrete particles in the argillaceous matrix ( Figure 3K,L). Inertinite (type-IV kerogen, derived from terrestrial plant tissues) consists of semifusinite, fusinite ( Figure 3M), micrinite and inertodetrinite, and has bright white color under the reflected light. Liptinite (type-II kerogen, transformed from plant organs) is relatively rare in the analyzed samples. Only some cutinite ( Figure 3N) and bituminite with obvious fluorescence characteristics are seen. Thus, it can be seen that the organic matter found in ORCs is mainly derived from terrestrial higher plants.

Description
The facies association I is composed of Gc, Sm, St, Sp, Sr, Fl, Si, Fr, and C ( Figure 4A). The sandstones are characterized by large thickness, intercalated with thin layers of siltstone and mudstone. Sedimentary structures such as basal erosional surface, massive bedding, cross-bedding, parallel bedding, and wavy bedding are well developed. Overall, the sandstones of facies association I have a fining-upward trend and a bell-shaped or jugged box-shaped logging curve ( Figure 4A). On the erosion surfaces, the organic-rich clasts are most concentrated, which are poorly sorted, angular to sub-angular, and chaotic ( Figure 4B,E-G,K). In the middle parts of the sand body, the floating ORC is scattered with long-axis tending towards bed-parallel orientations, mostly the shape of slender and deformed ( Figure 4C,J,L). The occurrence of small granule ORC is in the form of aggregates as discontinuous or continuous laminations in the upper parts ( Figure 4D,H Figure 4A). The sandstones are characterized by large thickness, intercalated with thin layers of siltstone and mudstone. Sedimentary structures such as basal erosional surface, massive bedding, cross-bedding, parallel bedding, and wavy bedding are well developed. Overall, the sandstones of facies association I have a fining-upward trend and a bell-shaped or jugged box-shaped logging curve ( Figure 4A). On the erosion surfaces, the organic-rich clasts are most concentrated, which are poorly sorted, angular to sub-angular, and chaotic (Figure 4B,E-G,K). In the middle parts of the sand body, the floating ORC is scattered with long-axis tending towards bed-parallel orientations, mostly the shape of slender and deformed ( Figure 4C,J,L). The occurrence of small granule ORC is in the form of aggregates as discontinuous or continuous laminations in the upper parts ( Figure 4D,H,I). These clasts are flaky, good sorted and rounded, coexisting with high fine-grained sediment content ( Figure 4C,J,M).

Interpretation
Thick sand sediments in the facies association I are interpreted as fluvial or distributary channel deposits ( Figure 4N), while fine-grained plant remnants in flood plain and mire provide the source for the formation of ORC, all developing in the Shanxi Formation. The ORCs in sandstone are chiefly the products of either: (1) scouring of the bottom underlying semi-consolidated peat by the high energy turbulent flow; (2) lateral erosion or slumping of bank sediments triggered by the water flow (high-density turbidity or quasi-stable flow). The ORC from different parts in sandstone underwent different sedimentation. Only a small amount of produced ORCs is similarly in-situ deposited in the vicinity of the erosion surface or after short-distance rolling transport. However, most of the produced ORCs are carried away and reworked by the water flow and water-transported debris [68]. The scattered floating ORC is the result of hindered setting in a high-density turbulent flow. After intense modification and long-distance transport, the ORC breaks up into small pieces of high maturity and deposits as the energy of the water flow diminishes. The loaded ORC, in the form of weakly continuous cross-lamination, is formed under the condition of transitional to high flow regime. In the low flow regime, the fragmented ORC is shaped into the continuous lamellar aggregate.   Interpretation Thick sand sediments in the facies association I are interpreted as fluvial or distributary channel deposits ( Figure 4N), while fine-grained plant remnants in flood plain and mire provide the source for the formation of ORC, all developing in the Shanxi Formation. The ORCs in sandstone are chiefly the products of either: (1) scouring of the bottom underlying semi-consolidated peat by the high energy turbulent flow; (2) lateral erosion or slumping of bank sediments triggered by the water flow (high-density turbidity or quasi-stable flow). The ORC from different parts in sandstone underwent different sedimentation. Only a small amount of produced ORCs is similarly in-situ deposited in the vicinity of the erosion surface or after short-distance rolling transport. However, most of the produced ORCs are carried away and reworked by the water flow and water-transported debris [68]. The scattered floating ORC is the result of hindered setting in a high-density turbulent flow. After intense modification and long-distance transport, the ORC breaks up into small pieces of high maturity and deposits as the energy of the water flow diminishes. The loaded ORC, in the form of weakly continuous cross-lamination, is formed under the condition of transitional to high flow regime. In the low flow regime, the fragmented ORC is shaped into the continuous lamellar aggregate.

Description
This facies association is built up of Sm, Sr, Si, Fl, and C ( Figure 5A). The thickness of Sm and Sr ranges between 1 and 3 m. Sandstones have an upward-coarsening trend with sharp contacts at the bottom, as well as a finger-shaped logging curve ( Figure 5A). Massive bedding, wavy bedding, and lenticular bedding can be observed. Also, roots can be recognized in the mudstone ( Figure 5B,D,F,H,I). The ORC in facies association II is generally subrounded, which range in size between granule and pebble (2~64 mm; Figure 5I). The scattered clasts distribute in the massive host sandstone (Sm; Figure 5H,I). In the upper parts, wavy lamina or thin intercalated aggregates of granule ORC are often observed ( Figure 5B,C).

Facies Association II Description
This facies association is built up of Sm, Sr, Si, Fl, and C ( Figure 5A). The thickness of Sm and Sr ranges between 1 and 3 m. Sandstones have an upward-coarsening trend with sharp contacts at the bottom, as well as a finger-shaped logging curve ( Figure 5A). Massive bedding, wavy bedding, and lenticular bedding can be observed. Also, roots can be recognized in the mudstone ( Figure  5B,D,F,H,I). The ORC in facies association II is generally subrounded, which range in size between granule and pebble (2~64 mm; Figure 5I). The scattered clasts distribute in the massive host sandstone (Sm; Figure 5H,I). In the upper parts, wavy lamina or thin intercalated aggregates of granule ORC are often observed ( Figure 5B,C).

Interpretation
Multilayered thin sandstone within this facies association developed by the channel burst in the effect of flood, identified as the crevasse splay ( Figure 5J). The ORCs are derived from the organic sediments at the channel bank or the initial area in which flood flow through ( Figure 5D-F). The scouring of a high-density flood, which has a fast flow rate and high energy, is the main reason for the organic-rich sediments turn into ORC in the special sedimentary environment. Due to the strong agitation of high-energy flood, ORC has a high degree of fragmentation and low structural maturity, rarely resulting in large blocks. The energy of flood decreases rapidly as a result of uncontained condition so that the ORC is deposited along with the sandy sediments after short-distance transportation. After the waters receded, the small ORC under the buoyant handling deposit as the thin layers.

Interpretation
Multilayered thin sandstone within this facies association developed by the channel burst in the effect of flood, identified as the crevasse splay ( Figure 5J). The ORCs are derived from the organic sediments at the channel bank or the initial area in which flood flow through ( Figure 5D-F). The scouring of a high-density flood, which has a fast flow rate and high energy, is the main reason for the organic-rich sediments turn into ORC in the special sedimentary environment. Due to the strong agitation of high-energy flood, ORC has a high degree of fragmentation and low structural maturity, rarely resulting in large blocks. The energy of flood decreases rapidly as a result of uncontained condition so that the ORC is deposited along with the sandy sediments after short-distance transportation. After the waters receded, the small ORC under the buoyant handling deposit as the thin layers.

Description
The facies association III comprises Gm, Sm, Sr, Sh, Fl, Si, Fr, and C ( Figure 6A). The sandstone body is developed in a multi-period, with a cumulative thickness of more than 15 m. Massive bedding, wavy bedding, and parallel bedding are main sedimentary structures. The GR logging curve is finger-shaped with some fluctuation ( Figure 6A). The ORC in this facies association is characterized by variable size (granules to boulders; 2 to >256 mm) and shape, angular nature and plastic deformation. At the bottom parts of the single sand body, the clasts are disorderly accumulated with gravel or coarse sand matrix ( Figure 6H). The floating clasts are isolated occurring in the structureless host sandstone, with strong deformation and long-axis running parallel to bed ( Figure 6B,C,E-G,I,K). The small granule clasts are clustered in the form of wavy or parallel laminations ( Figure 6J). The facies association III comprises Gm, Sm, Sr, Sh, Fl, Si, Fr, and C ( Figure 6A). The sandstone body is developed in a multi-period, with a cumulative thickness of more than 15 m. Massive bedding, wavy bedding, and parallel bedding are main sedimentary structures. The GR logging curve is finger-shaped with some fluctuation ( Figure 6A). The ORC in this facies association is characterized by variable size (granules to boulders; 2 to >256 mm) and shape, angular nature and plastic deformation. At the bottom parts of the single sand body, the clasts are disorderly accumulated with gravel or coarse sand matrix ( Figure 6H). The floating clasts are isolated occurring in the structureless host sandstone, with strong deformation and long-axis running parallel to bed ( Figure 6B,C,E-G,I,K). The small granule clasts are clustered in the form of wavy or parallel laminations ( Figure 6J).

Interpretation
Thick sandstone with ORC in the sequence is interpreted as the deposits of the tidal channel ( Figure 6L), mostly distributed in the upper Benxi and Taiyuan Formations. The formation of ORC, whose precursors are mainly organic-rich deposits in marsh or lagoon, is controlled by tidal processes, including basal erosion, bank erosion, and slump. With the changes in the positional relationship between the sun, the moon and the earth, the energy of tide has the characteristic of periodic variations. The channel-bottom deposits are flood dominated, with irregular, poorly sorted ORC mixed with gravel or coarse sand. Some large particles transported by tidal turbulence probably trapped and deposited in singles within the massive sandstone, usually resulting in heavy bending and deforming ( Figure 6B,K). When the channel is ebb dominated, tidal energy gradually weakens,

Interpretation
Thick sandstone with ORC in the sequence is interpreted as the deposits of the tidal channel ( Figure 6L), mostly distributed in the upper Benxi and Taiyuan Formations. The formation of ORC, whose precursors are mainly organic-rich deposits in marsh or lagoon, is controlled by tidal processes, including basal erosion, bank erosion, and slump. With the changes in the positional relationship between the sun, the moon and the earth, the energy of tide has the characteristic of periodic variations. The channel-bottom deposits are flood dominated, with irregular, poorly sorted ORC mixed with gravel or coarse sand. Some large particles transported by tidal turbulence probably trapped and deposited in singles within the massive sandstone, usually resulting in heavy bending and deforming ( Figure 6B,K). When the channel is ebb dominated, tidal energy gradually weakens, and the small granule ORC transported by buoyancy tends to deposit as laminations in wavy bedding sandstone ( Figure 6J).

Description
The facies association IV is characterized by more internal structures containing Sr, Fl, Si, Fr, and C ( Figure 7A). Fine-grained sediments and coal are developed extensively, while sandy sediments range in thickness between 0.5 and 2 m. It is quite common to see tidal bedding such as flaser bedding, wavy bedding and lenticular bedding ( Figure 7G,I-K), as well as various bioturbation structures ( Figure 7F,H). The coaly fragments and plant pieces, predominantly sub-rounded to rounded, are common in the sandstone. The size of these clasts are in range from small pebbles to large cobbles (4~256 mm), occasionally boulders ( Figure 7C). The most common occurrence of ORC is loaded as the wavy discontinuous lamination ( Figure 7B-D).
Energies 2020, 13, x FOR PEER REVIEW 11 of 19 range in thickness between 0.5 and 2 m. It is quite common to see tidal bedding such as flaser bedding, wavy bedding and lenticular bedding ( Figure 7G,I-K), as well as various bioturbation structures ( Figure 7F,H). The coaly fragments and plant pieces, predominantly sub-rounded to rounded, are common in the sandstone. The size of these clasts are in range from small pebbles to large cobbles (4~256 mm), occasionally boulders ( Figure 7C). The most common occurrence of ORC is loaded as the wavy discontinuous lamination ( Figure 7B-D).

Interpretation
Thin wavy bedding sandstone of this facies association typifies the sand flat deposit in a tidal flat environment ( Figure 7N). The thick coal seams and organic-rich mud shales ( Figure 7L,M), which develop in marsh and lagoon, supply sufficient source for ORC. Two main mechanisms exist on the formation of ORC: basal erosion under the effect of tide and detachment due to synaeresis cracking ( Figure 7I,M), while the transport of the broken ORC from the origin site is operated by the processes of tide currents. At the level of high tide, some large particles of ORC are trapped by sandy deposits; whereas most ORC would break up repeatedly under the action of tide currents. With the ebb of tide, the residual granule ORC would load and form into wavy lamellar aggregates. The circular coaly ORC, having a grain size of >10 cm in Figure 7C, should be a cross-section of the plant stem, which probably formed directly after depositing in the sand.

Facies Association V Description
The fine-to-medium sandy sediments are the major component of facies association V, while the gravels barely exist ( Figure 8A). They display bed with a succession of Sm, Sh, Si, and Fr. Massive bedding and parallel bedding can be recognized generally. Moreover, the overall sandstone body

Interpretation
Thin wavy bedding sandstone of this facies association typifies the sand flat deposit in a tidal flat environment ( Figure 7N). The thick coal seams and organic-rich mud shales ( Figure 7L,M), which develop in marsh and lagoon, supply sufficient source for ORC. Two main mechanisms exist on the formation of ORC: basal erosion under the effect of tide and detachment due to synaeresis cracking ( Figure 7I,M), while the transport of the broken ORC from the origin site is operated by the processes of tide currents. At the level of high tide, some large particles of ORC are trapped by sandy deposits; whereas most ORC would break up repeatedly under the action of tide currents. With the ebb of tide, the residual granule ORC would load and form into wavy lamellar aggregates. The circular coaly ORC, having a grain size of >10 cm in Figure 7C, should be a cross-section of the plant stem, which probably formed directly after depositing in the sand.

Description
The fine-to-medium sandy sediments are the major component of facies association V, while the gravels barely exist ( Figure 8A). They display bed with a succession of Sm, Sh, Si, and Fr. Massive bedding and parallel bedding can be recognized generally. Moreover, the overall sandstone body develops multi-cycle erosion surfaces with fining-upward. The ORCs are mainly mudstone (shale) breccias ( Figure 8C,D,F,G,I), but rarely coaly fragments and plant pieces. The intact boulder ORC retains the horizontal bedding of shale ( Figure 8C,G). These clasts are angular to sub-rounded, with the characteristic of imbricate arrangement. The long axis of the particles is generally parallel or sub-parallel to the bedding. On the surface of basal erosion, ORCs are accumulated in variable shape and size (small pebbles to boulders; Figure 8C,F,H). In the middle parts of the single sandstone body, long strip or flaky clasts are sporadically floating in structureless sandstone ( Figure 8D,E,I,J). The finely rounded pebble ORCs are deposited in weak continuous parallel laminations at the upper parts ( Figure 8B).

Interpretation
Facies association V is limited in the lower Benxi Formation, representing the deposition of the sandy debris or turbidity flow controlled by the topography of the underlying Ordovician weathering crust locally ( Figure 8K). In this case, the ORC is probably owing to flow basal erosion of muddy bottom or flow-triggered failure of muddy slope. The thick clast-supported Sm together with the presence of intact boulder ORC indicates the processes of high-energy water flow. The ORCs carried by rolling movement at the bottom of dense flow deposits first, with a typical feature of very low textural maturity for short-distance transportation ( Figure 8C,F-I). Subsequently, some of the ORCs lifted by turbulence will overcome the limitation of buoyancy and deposit individually or in groups, which orient in the long-axis direction ( Figure 8D,E,J). The ORCs, carried by high-dense flow far and modified strongly, deposit with the weakening of flow energy and transporting capacity ( Figure 8B).

Occurrence and Classification
The development of ORCs in coal-bearing sandstone is an important geological phenomenon which cannot be ignored. The occurrence of ORCs is not only influenced by the transportation of water flow, but also related to their own composition [2,12,30]. The hydrodynamic conditions of the water flow control the transportation process of ORCs (including the transportation ways, the transportation distance and the reworking intensity), which determines the final sedimentary style of ORCs, specific performances: (1) Some rolling transported ORCs have a short transportation

Interpretation
Facies association V is limited in the lower Benxi Formation, representing the deposition of the sandy debris or turbidity flow controlled by the topography of the underlying Ordovician weathering crust locally ( Figure 8K). In this case, the ORC is probably owing to flow basal erosion of muddy bottom or flow-triggered failure of muddy slope. The thick clast-supported Sm together with the presence of intact boulder ORC indicates the processes of high-energy water flow. The ORCs carried by rolling movement at the bottom of dense flow deposits first, with a typical feature of very low textural maturity for short-distance transportation ( Figure 8C,F-I). Subsequently, some of the ORCs lifted by turbulence will overcome the limitation of buoyancy and deposit individually or in groups, which orient in the long-axis direction ( Figure 8D,E,J). The ORCs, carried by high-dense flow far and modified strongly, deposit with the weakening of flow energy and transporting capacity ( Figure 8B).

Occurrence and Classification
The development of ORCs in coal-bearing sandstone is an important geological phenomenon which cannot be ignored. The occurrence of ORCs is not only influenced by the transportation of water flow, but also related to their own composition [2,12,30]. The hydrodynamic conditions of the water flow control the transportation process of ORCs (including the transportation ways, the transportation distance and the reworking intensity), which determines the final sedimentary style of ORCs, specific performances: (1) Some rolling transported ORCs have a short transportation distance and low degree of re-working within the dense flow, chaotically accumulating above the erosion surface with low texture maturity ( Figure 9J-L). (2) The jumping transported ORCs are subjected to the strong hydrodynamic forces. Some large and intact ORCs are caught in the rapidly deposited sandy sediments leading to the severe plastic deformation ( Figure 9G-I); some ORCs that "survived" from the actions of water flow and the collisions of grains (mostly sandy sediments) are small-sized but numerous with good sorting and roundness ( Figure 9D-F); but the others are completely disintegrated during the transportation.
(3) Some suspended and lightweight ORCs are transported over long distance with relatively weak reworking degree, and deposited as thin interlayers together with fine-grained sediments (mainly silts and clays) under weak hydrodynamic conditions ( Figure 9A-C). The composition of ORCs also has an important influence on their susceptibility to mechanical disintegration [30]. The ORCs are mainly composed of higher plant debris Under the action of water flow, some muddy ORCs can be completely disintegrated into clay particles after undergoing mechanical attrition and disintegration; while higher plant fragments only change from large to small particles.  The classification of ORCs proposed here is based on considerations of their occurrence and the characteristics of hosting sediments. The characteristics given in Figure 8 and Table 2 are designed to aid in identification and interpretation with different types of ORCs. The energy of water flow changes dynamically, resulting in its different transportation mechanism at different stages [5,12,69]. Under a range of its processes, the vertical distribution characteristic of ORCs in coal-bearing sandstone confirms to the law of mechanical sedimentary differentiation. As the energy and transporting capacity of single water flow changes from strong to weak, the sedimentary sequences of ORCs can be concluded from the bottom up as follows: diamictic organic-rich clasts (ORC-1), floating organic-rich clasts (ORC-2), loaded lamellar organic-rich clasts (ORC-3) and thin interlayer The classification of ORCs proposed here is based on considerations of their occurrence and the characteristics of hosting sediments. The characteristics given in Figure 8 and Table 2 are designed to aid in identification and interpretation with different types of ORCs. The energy of water flow changes dynamically, resulting in its different transportation mechanism at different stages [5,12,69].
Under a range of its processes, the vertical distribution characteristic of ORCs in coal-bearing sandstone confirms to the law of mechanical sedimentary differentiation. As the energy and transporting capacity of single water flow changes from strong to weak, the sedimentary sequences of ORCs can be concluded from the bottom up as follows: diamictic organic-rich clasts (ORC-1), floating organic-rich clasts (ORC-2), loaded lamellar organic-rich clasts (ORC-3) and thin interlayer organic-rich clasts (ORC-4, listed in Table 2, Figure 9). From ORC-1 to ORC-4, the grain size of their hosting sandy sediments shows a change from coarse to fine (Figure 9), which also confirms a vertical differentiation of ORCs. However, these four types of ORCs can occur differently in different facies associations or not developed originally in part, depending on the actual conditions in a special geological environment.

Formation Mechanism
The Upper Paleozoic sedimentary period in the Ordos Basin is in the background of transgression, and ORC is generated under the water action from rivers, tides, waves, and episodically floods and debris flows ( Figure 10). The formation process of ORC underwater flow can be distinguished into four stages in sequence: (1) Original sedimentation of organic matter and fine-grained sediments to form source; (2) detachment of organic-rich sediments under hydrodynamism, which includes two main mechanisms: one is the basal erosion resulting in high-energy water flow, and the other is the instability slope failure triggered by water flow vibration; (3) transportation and reworking by water flow and water-transported debris; among them, the reworking is a dynamic process, including multiple crushing, deformation (such as squeezing squashing folding pressing), sorting, rounding; (4) allogenic re-deposition [1,2]. The initial failure products of organic-rich sediments are irregular ORC blocks, while transportation by water flow is the determinant of the difference in ORC deposition characteristics [1,2,30]. Based on this, we propose that the formation mechanisms of ORC could be classified into: long-term altering of continuous water flow (such as fluvial water, tide, etc.) and short-term water flow acting triggered by sudden events (such as flood, debris flow, etc.).
Energies 2020, 13, x FOR PEER REVIEW 15 of 19 slow but gradual process. In the lower flow regime, the suspended ORC often deposits as thin interlayers with fine-grained muddy sediments, usually neglecting the role of ORC previously. Interestingly, the modification degree of transport on ORC in the short-term water flow is less than the first type, typically low textual maturity. The temporary water flow is often triggered by a sudden event, which may be flood, earthquake, storm or tsunami. This water flow tends to be highenergy, high-density and dissipates energy rapidly (often lasting only a few hours) for breaking through the confined state, resulting in the weak re-working on ORC during transportation. In this study, the thick-bedded diamictic ORC deposited in the early stage of the high-energy water flow energy weakening. Where after, some ORCs were captured during the deposition of sandy sediments, transported in skipping. Finally, the ORCs contained in the suspension transport formed thin interlayers in a lower flow regime, but it is seldom recognized. There are two major reasons: the basal erosion by the new sudden water flow or continuous deposition with fine-grained deposits in the absence of new sudden water flow.

Conclusions
(1) It is proposed to use the descriptive vocabulary organic-rich clasts (ORC) to collectively represent carbonaceous fragments, carbonaceous mudstone clasts, shale clasts, dark mudstone clasts and plant fragments developed in coal-bearing sandstones.
(2) A total of five sedimentary environments of ORC were identified, including fluvial channels, crevasse fans, tidal channels, sand flats, and subaqueous debris flow deposits.
(3) The occurrence of ORCs in coal-bearing sandstones is not only controlled by the changes of the water flow during transportation, but also related to the decomposition resistance of their components. After a series of processes during water flow transport, ORCs shows the characteristic of obvious mechanical differentiation in the vertical direction. Based on this, we propose that ORCs can be classified into four types: diamictic organic-rich clasts, floating organic-rich clasts, loaded lamellar organic-rich clasts, and thin interlayer organic-rich clasts.
(4) The changes in water flow energy during transportation play a controlling role in the formation of ORCs. We have summarized two formation mechanisms of ORCs in coal-bearing sandstones, including the long-term altering of continuous water flow and the short-term water flow acting triggered by sudden events.  Regarding the first instance, the sedimentary characteristics of the residual ORC in the coal-bearing sandstone are the results of modification by the continuous or periodic water flow within a long period. In the process of transportation, ORCs undergo a series of dynamic processes including liquefying, crushing, squeezing, squashing, winnowing, folding and pressing in the long-term and repeatedly, resulting in broken-up of most pre-formed ORC into smaller fragments. The vertical differentiation between sandy sediments and organic-rich debris is obvious, which suggests that the evolution of water flow from high-density, high-energy to low-density; low-energy turbulence is a slow but gradual process. In the lower flow regime, the suspended ORC often deposits as thin interlayers with fine-grained muddy sediments, usually neglecting the role of ORC previously.
Interestingly, the modification degree of transport on ORC in the short-term water flow is less than the first type, typically low textual maturity. The temporary water flow is often triggered by a sudden event, which may be flood, earthquake, storm or tsunami. This water flow tends to be high-energy, high-density and dissipates energy rapidly (often lasting only a few hours) for breaking through the confined state, resulting in the weak re-working on ORC during transportation. In this study, the thick-bedded diamictic ORC deposited in the early stage of the high-energy water flow energy weakening. Where after, some ORCs were captured during the deposition of sandy sediments, transported in skipping. Finally, the ORCs contained in the suspension transport formed thin interlayers in a lower flow regime, but it is seldom recognized. There are two major reasons: the basal erosion by the new sudden water flow or continuous deposition with fine-grained deposits in the absence of new sudden water flow.

Conclusions
(1) It is proposed to use the descriptive vocabulary organic-rich clasts (ORC) to collectively represent carbonaceous fragments, carbonaceous mudstone clasts, shale clasts, dark mudstone clasts and plant fragments developed in coal-bearing sandstones.
(2) A total of five sedimentary environments of ORC were identified, including fluvial channels, crevasse fans, tidal channels, sand flats, and subaqueous debris flow deposits.
(3) The occurrence of ORCs in coal-bearing sandstones is not only controlled by the changes of the water flow during transportation, but also related to the decomposition resistance of their components. After a series of processes during water flow transport, ORCs shows the characteristic of obvious mechanical differentiation in the vertical direction. Based on this, we propose that ORCs can be classified into four types: diamictic organic-rich clasts, floating organic-rich clasts, loaded lamellar organic-rich clasts, and thin interlayer organic-rich clasts.
(4) The changes in water flow energy during transportation play a controlling role in the formation of ORCs. We have summarized two formation mechanisms of ORCs in coal-bearing sandstones, including the long-term altering of continuous water flow and the short-term water flow acting triggered by sudden events.