Gcm |
Massive or crudely-stratified clast-supported to sandy matrix-supported conglomerates with a coarse sandstone “matrix”, composed of subangular to subrounded granules and pebbles of polymitic fragments (gneiss, schist, granite, quartz and feldspars). Millimetric plant fragments occur locally. Beds range from 10 cm to 1 m in thickness, frequently with an abrupt base. Fig. 4A. |
Pseudoplastic debris flow (inertial bedload, turbulent flow); rarely, longitudinal bedforms (Miall 2006Miall A.D. 2006. The Geology of Fluvial Deposits: Sedimentary Facies, Basin Analysis, and Petroleum Geology. Berlin, Springer, 582 p.). |
Gmm |
Massive matrix-supported conglomerates (locally gravelly mudstones) composed of a mudstone matrix with dispersed subangular to subrounded granules and pebbles of polymitic fragments (gneiss, schist, granite, quartz and feldspars). Dish and pillar structures and diagenetic sideritic (?) nodules (< 1 cm) can occur. Beds range from 5 cm to 8 m in thickness. Fig. 4B. |
Plastic debris flow (high-strength, viscous) (Miall 2006Miall A.D. 2006. The Geology of Fluvial Deposits: Sedimentary Facies, Basin Analysis, and Petroleum Geology. Berlin, Springer, 582 p.). |
Gmi
|
Massive or with faint horizontal lamination coarse-grained sandstones to clast-supported conglomerates, poorly to moderately-sorted, composed of millimetric to centimetric intraclasts and subangular granules of immature composition (quartz, feldspars and lithic fragments). Beds range from 1 to 35 cm in thickness and may locally present normal grading. Abrupt and erosive top and base and heterolithic intercalations are common. Fig. 4C. |
Reworking of sediments with some lithification in high hydrodynamic conditions by strong subaqueous tractive current (lag deposits) (Holz, 2003Holz M. 2003. Sequence stratigraphy of a lagoonal estuarine system-an example from the lower Permian Rio Bonito Formation, Paraná Basin, Brazil. Sedimentary Geology, 162(3):305-331. http://dx.doi.org/10.1016/S0037-0738(03)00156-8
http://dx.doi.org/10.1016/S0037-0738(03)...
; Plint, 2010Plint A.G. 2010. Wave- and storm-dominated shoreline and shallow-marine systems. In: James N.P., Dalrymple R. W. (Eds.), Facies models 4. Newfoundland & Labrador, Geological Association of Canada Publications, 4, p. 167-199.; Zecchin et al., 2017Zecchin M., Caffau M., Catuneanu O., Lenaz D. 2017. Discrimination between wave‐ravinement surfaces and bedset boundaries in Pliocene shallow‐marine deposits, Crotone Basin, southern Italy: An integrated sedimentological, micropalaeontological and mineralogical approach. Sedimentology, 64(7):1755-1791. https://doi.org/10.1111/sed.12373
https://doi.org/10.1111/sed.12373...
). |
Sm |
Very fine- to very coarse-grained, moderately to poorly-sorted massive sandstones, usually presenting normal grading. Centimetric to millimetric bioturbation (BI: 1 to 4; vertical, subvertical and horizontal excavations), dish and pillar structures and millimetric mud films are usual features. Dispersed subangular granules and pebbles of quartz and lithic fragments, millimetric plant fragments, mud intraclasts (< 4 cm), diagenetic sideritic (?) nodules (< 1 cm) and synsedimentary folds occur locally. Beds range from 10 cm to 2 m in thickness and rarely present an abrupt base contact. Fig. 4D. |
Rapid deposition of hyperconcentrated flows, fluidization, intensive bioturbation and high compaction during diagenesis (Miall 2006Miall A.D. 2006. The Geology of Fluvial Deposits: Sedimentary Facies, Basin Analysis, and Petroleum Geology. Berlin, Springer, 582 p.). |
Sc |
Very coarse- to fine-grained, poorly to well-sorted sandstones with cross-stratification, locally presenting normal grading. Dispersed subangular granules and pebbles of quartz and lithic fragments, millimetric mud films, (< 3 cm), plant fragments (< 1 cm) and diagenetic sideritic (?) nodules (< 1 cm) occur locally. Mud intraclasts and synsedimentary folds are rare. Beds range from 15 cm to 9 m in thickness and locally present an abrupt basal contact. Fig. 4E. |
Migration of subaqueous sandy dunes in unidirectional lower flow regime (Allen 1963Allen J.R.L. 1963. The classification of cross-stratified units, with notes on their origin. Sedimentology, 2(2):93-114. https://doi.org/10.1111/j.1365-3091.1963.tb01204.x
https://doi.org/10.1111/j.1365-3091.1963...
, Collinson et al. 2006Collinson J.D., Mountney N., Thompson D.B. 2006. Sedimentary Structures. Hertfordshire, Terra Publishing, 292 p.). |
Scd
|
Coarse- to fine-, rarely very coarse-grained, poorly to well-sorted sandstones with cross-stratification, commonly presenting normal grading. Regular to irregular millimetric single mud drapes (rarely double mud drapes), mud intraclasts (< 4 cm) and plant fragments (< 1 cm) are usual features. Millimetric to centimetric bioturbation (BI: 1; horizontal excavation) and dish and pillar structures are rare. Beds range from 15 cm to 0.5 m in thickness and rarely present an abrupt contact. Fig. 4F. |
Alternating traction process with migration of subaqueous sandy dunes in lower flow regime and deposition by settling down of suspensed load in standing water (Visser 1980Visser M.J. 1980. Neap-spring cycles reflected in Holocene subtidal large-scale bedform deposits: a preliminary note. Geology, 8(11):543-546. https://doi.org/10.1130/0091-7613(1980)8%3C543:NCRIHS%3E2.0.CO;2
https://doi.org/10.1130/0091-7613(1980)8...
). |
Shcs |
Fine-, rarely medium-grained, moderately to well-sorted sandstones presenting hummocky cross-stratification. Centimetric to millimetric bioturbations (BI: 1 to 6; horizontal and vertical excavations) are common and beds range from 20 cm to 9.05 m in thickness. Fig. 4G. |
Settling of suspended sediments under low energy oscillatory-dominant, combined flow (distal tempestite deposition) (Harms et al. 1975Harms J.C., Southard J.B., Spearing D.R., Walker R.G. 1975. Depositional environments as interpreted from primary sedimentary structures and stratification sequences. Short Course n. 2, SEPM, p. 161., Dumas & Arnott 2006Dumas S., Arnott R.W.C. 2006. Origin of hummocky and swaley cross-stratification - the controlling influence of unidirectional current strength and aggradation rate. Geology, 34(12):1073-1076. https://doi.org/10.1130/G22930A.1
https://doi.org/10.1130/G22930A.1...
). |
Sscs |
Fine- to medium-grained, moderately to well-sorted sandstones with swaley cross-stratification, locally presenting normal grading. Centimetric mud films are common and beds range from 20 cm to 7.4 m in thickness. Fig. 4H. |
Settling of suspended sediments under high-energy oscillatory-dominant, combined flow (proximal tempestite deposition as amalgamated hummocky cross-stratification deposit) (Harms et al. 1975Harms J.C., Southard J.B., Spearing D.R., Walker R.G. 1975. Depositional environments as interpreted from primary sedimentary structures and stratification sequences. Short Course n. 2, SEPM, p. 161., Dumas & Arnott 2006Dumas S., Arnott R.W.C. 2006. Origin of hummocky and swaley cross-stratification - the controlling influence of unidirectional current strength and aggradation rate. Geology, 34(12):1073-1076. https://doi.org/10.1130/G22930A.1
https://doi.org/10.1130/G22930A.1...
). |
Sh |
Fine- to medium-, rarely very fine-grained, poorly to well-sorted sandstones presenting horizontal to low angle cross-stratification. Millimetric plant fragments, mud intraclasts and discontinuous mud films are common and millimetric to centimetric bioturbations (BI: 2; vertical excavations) are rare. Beds range from 10 cm to 2.1 m in thickness. Fig. 4I. |
Attenuated bedforms in transition between lower and upper flow regime (Best & Bridge 1992Best J.L., Bridge J.S. 1992. The morphology and dynamics of low amplitude bedwaves upon stage plane beds and the preservation of planar laminae. Sedimentology, 39(5):737-752. https://doi.org/10.1111/j.1365-3091.1992.tb02150.x
https://doi.org/10.1111/j.1365-3091.1992...
, Miall 2006Miall A.D. 2006. The Geology of Fluvial Deposits: Sedimentary Facies, Basin Analysis, and Petroleum Geology. Berlin, Springer, 582 p.). |
Sr |
Fine- to medium-grained, moderately to well-sorted sandstones presenting unidirectional, rarely bidirectional (proportion of 1/10) ripple cross-lamination. Millimetric mud films and plant fragments can occur. Beds range from 15 cm to 1.5 m in thickness. Fig. 4J. |
Migration of subaqueous ripples in unidirectional (rarely anisotrophic bidirectional) lower flow regime (Allen 1963Allen J.R.L. 1963. The classification of cross-stratified units, with notes on their origin. Sedimentology, 2(2):93-114. https://doi.org/10.1111/j.1365-3091.1963.tb01204.x
https://doi.org/10.1111/j.1365-3091.1963...
, Miall 2006Miall A.D. 2006. The Geology of Fluvial Deposits: Sedimentary Facies, Basin Analysis, and Petroleum Geology. Berlin, Springer, 582 p.). |
Srd
|
Fine- to medium-grained, moderately- to well-sorted sandstones presenting unidirectional, rarely bidirectional (proportion of 1/10), ripple cross-lamination and regular to irregular millimetric single mud drapes (rarely double mud drapes). Millimetric plant fragments and bioturbation (BI: 2 to 3; mostly horizontal excavations) can occur. Beds range from 55 cm to 1.6 m in thickness. Fig. 4k. |
Alternating traction process with migration of subaqueous ripples in unidirectional (rarely anisotrophic bidirectional) lower flow regime and deposition by settling down of suspensed load in standing water (Visser 1980Visser M.J. 1980. Neap-spring cycles reflected in Holocene subtidal large-scale bedform deposits: a preliminary note. Geology, 8(11):543-546. https://doi.org/10.1130/0091-7613(1980)8%3C543:NCRIHS%3E2.0.CO;2
https://doi.org/10.1130/0091-7613(1980)8...
). |
Sw |
Fine-, rarely medium- or coarse-grained, moderately to well-sorted sandstones presenting wave- (rarely combined) ripple cross-lamination. Millimetric to centimetric mud films are common features and centimetric to millimetric bioturbations (BI: 2 to 3; mostly horizontal excavations) are rare. Diagenetic sideritic (?) nodules (< 1 cm) and millimetric mud intraclasts may occur. Beds range from 10 cm to 2.35 m in thickness. Fig. 4L. |
Symmetrical (or asymmetrical) ripples in oscillatory (or oscillatory and traction) lower flow regime (Walker & Plint 1992Walker R.G., Plint A.G. 1992. Wave- and storm-dominated shallow marine systems. In: Walker R.G., James N.P. (Eds.). Facies Models - Response to Sea Level Change. Newfoundland, Geological Association of Canada Publications, p. 219-238., Clifton 2006Clifton H.E. 2006. A reexamination of facies models for clastic shorelines. In: Posamentier H.W., Walker R.G. (Eds.), Facies Models Revisited. Tulsa, Society for Sedimentary Geology, p. 293-336.). |
Hr |
Heterolithic intercalations of very fine-grained sandstones with mudstones varying from wavy, lenticular to flaser bedding. Occurrence of unidirectional ripple cross-lamination in sandy portions and thin parallel lamination in muddy levels. Millimetric to centimetric bioturbations (BI: 1 to 4; mostly horizontal excavations), plant fragments (< 1 cm), diagenetic sideritic (?) nodules (< 1 cm) and dish and pillar structures are common features. Beds range from 15 cm to 2.75 m in thickness. Fig. 5A. |
Alternating traction process with subaqueous ripples in unidirectional lower flow regime and deposition by decantation of suspended load (Dalrymple 2010Dalrymple R.W. 2010. Tidal depositional systems. In: James N.P., Dalrymple R.W. (Eds.), Facies models 4. Newfoundland & Labrador, Geological Association of Canada Publications, 4, p. 201-231.). |
Hrb
|
Heterolithic intercalations of very fine- to fine-, rarely coarse and medium-grained sandstones with mudstones varying from wavy, lenticular to flaser bedding. Bidirectional (proportion of 1/10) ripples cross-lamination in sandy portions and thin parallel lamination in muddy levels can occur. Millimetric bioturbations (BI: 1 to 3; mostly horizontal excavations) are common. Basal abrupt contact, normal grading and disperse subangular granules and pebbles of quartz and lithic fragments occur locally. Beds range from 25 cm to 1.6 m in thickness. Fig. 5B. |
Alternating traction process with subaqueous ripples in anisotrophic bidirectional lower flow regime with deposition by decantation of suspended load (Dalrymple 2010Dalrymple R.W. 2010. Tidal depositional systems. In: James N.P., Dalrymple R.W. (Eds.), Facies models 4. Newfoundland & Labrador, Geological Association of Canada Publications, 4, p. 201-231.). |
Hw |
Heterolithic intercalations of very fine- to fine-grained sandstones with mudstones varying from wavy, lenticular to flaser bedding. Wave-ripple cross-lamination (locally combined-ripple cross-lamination) in sandy portions and thin parallel to wave lamination in muddy levels can occur. Millimetric bioturbations (BI: 3 to 4; mostly horizontal excavations) are very common and beds range from 15 cm to 18.3 m in thickness. Fig. 5C. |
Alternating oscillatory (sometimes combined-traction and oscillatory) process with symmetrical (sometimes asymmetrical) subaqueous ripples in lower flow regime and deposition by decantation of suspended load (Walker & Plint 1992Walker R.G., Plint A.G. 1992. Wave- and storm-dominated shallow marine systems. In: Walker R.G., James N.P. (Eds.). Facies Models - Response to Sea Level Change. Newfoundland, Geological Association of Canada Publications, p. 219-238., Clifton 2006Clifton H.E. 2006. A reexamination of facies models for clastic shorelines. In: Posamentier H.W., Walker R.G. (Eds.), Facies Models Revisited. Tulsa, Society for Sedimentary Geology, p. 293-336.). |
Fm |
Massive, medium to dark gray mudstones, locally in blocks and presenting incipient lamination. Plant fragments (0.2 to 2 cm) with variable distribution are common fratures and beds range from 30 cm to 4.8 min thickness. Fig. 5D. |
Lack of lamination due to (i) flocculation of clay suspension or (ii) loss of lamination associated intensive bioturbation or burial compaction (Miall 2006Miall A.D. 2006. The Geology of Fluvial Deposits: Sedimentary Facies, Basin Analysis, and Petroleum Geology. Berlin, Springer, 582 p., Foix et al. 2013Foix N., Paredes J.M., Giacosa R.E. 2013. Fluvial architecture variations linked to changes in accomodation space: río chico formation (late paleocene), golfo san jorge basin, Argentina. Sedimentary Geology, 294:342-355. http://dx.doi.org/10.1016/j.sedgeo.2013.07.001
http://dx.doi.org/10.1016/j.sedgeo.2013....
). |
Fl |
Medium grey mudstones with thin parallel lamination, locally interlayered with millimetric of very fine-grained sandstones. Plant fragments (0.2 to 2 cm) with variable distribution are common and dish and pillar structures, synsedimentary faults and millimetric bioturbations (BI: 1; horizontal excavations) are rare. Beds range from 5 cm to 1.8 m in thickness. Fig. 5E. |
Suspension settling, dominantly from standing water (Rogers & Astin 1991Rogers D.A., Astin T.R. 1991. Ephemeral lakes, mud pellets and wind-blown sand and silt: reinterpretations of Devonian lacustrine cycles in north Scotland. In: Anadon P., Cabrera L.L., Kelts K. (Eds.), Lacustrine Facies Analysis. Special Publication n. 13, IAS, p. 199-222.). |
C |
Coal, locally reddish black, with beds ranging from 5 to 45 cm in thickness. Fig. 5F. |
Decantation of high amounts of organic matter, mixed with clay minerals (less proportion), on subaqueous and reducing conditions; post-depositional oxidizing conditions (McCabe 1985McCabe P.J. 1985. Depositional environments of coal and coal‐bearing strata. In: Rahmani R.A., Flores R.M. (Eds.), Sedimentology of coal and coal‐bearing sequences. Oxford, IAS, Special Publication, 7, p.13-42.). |