Time-Transgressive Confinement On the Slope and the Progradation of Basin-Floor Fans: Implications For the Sequence Stratigraphy of Deep-Water Deposits

Hodgson, David M.; Kane, Ian A.; Flint, Stephen S.; Brunt, Rufus L.; Ortiz-Karpf, Andrea

doi:10.2110/jsr.2016.3

Cited by 91 publications

(118 citation statements)

References 104 publications

Supporting

Mentioning

109

Contrasting

Order By: Relevance

“…7). Younger lobe deposits of LC1 pinch-out successively farther to the north, which is 272 consistent with a progradational stacking pattern (sensu Hodgson et al, 2016), and frontal pinch-out 273 at the scale of a lobe. The frontal sand pinch-out of LC1 in the Sout Rivier area (Fig.…”

Section: Fan 4 Paleogeographic Reconstruction 266mentioning

confidence: 60%

Frontal and Lateral Submarine Lobe Fringes: Comparing Sedimentary Facies, Architecture and Flow Processes

Spychala¹,

Hodgson²,

Prélat³

et al. 2017

Journal of Sedimentary Research

Self Cite

116

144

View full text Add to dashboard Cite

13Submarine lobe fringe deposits form heterolithic successions that may include a high proportion of 14 hybrid beds. The identification of lobe fringe successions aids interpretation of paleogeographic 15 setting and the degree of basin confinement. Here, for the first time, the sedimentological and 16 architectural differences between frontal and lateral lobe fringe deposits are investigated. Extensive 17 outcrop and core data from Fan 4, Skoorsteenberg Formation, Karoo Basin, South Africa, allow the 18 rates and style of facies changes from axis to fringe settings of lobes and lobe complexes in both 19 down-dip (frontal) and across-strike (lateral) directions to be tightly constrained over a 800 km 2 20 study area. Fan 4 comprises three sand-prone divisions that form compensationally stacked lobe 21 complexes, separated by thick packages of thin-bedded siltstone and sandstone intercalated with 22 2 (muddy) siltstone, interpreted as the fringes of lobe complexes. Lobe-fringe facies associations 23 comprise: i) thick-bedded structureless or planar laminated sandstones that pinch and swell, and are 24 associated with underlying debrites; ii) argillaceous and mudclast-rich hybrid beds; and iii) current 25 ripple-laminated sandstones and siltstones. Typically, frontal fringes contain high proportions of 26 hybrid beds and transition from thick-bedded sandstones over length-scales of 1 to 2 km. In 27 contrast, lateral fringe deposits tend to comprise current ripple-laminated sandstones that transition 28 to thick-bedded sandstones in the lobe axis over several kilometers.

show abstract

Section: Fan 4 Paleogeographic Reconstruction 266mentioning

confidence: 60%

Frontal and Lateral Submarine Lobe Fringes: Comparing Sedimentary Facies, Architecture and Flow Processes

Spychala¹,

Hodgson²,

Prélat³

et al. 2017

Journal of Sedimentary Research

Self Cite

116

144

View full text Add to dashboard Cite

show abstract

“…6), indicating that deposition was not sufficiently sustained or sediment volume was not adequate for lobes to stack. Neither compensational stacking to form a lobe complex, nor propagation of channel-levee systems above lobes (e.g., Morris et al, 2014b;Hodgson et al, 2016) is documented in these units. In addition to thickness, A/B, B/C, and D/E show key differences in facies and architecture to the larger Units A-F (cf.…”

Section: Discussion Units A/b B/c and D/ementioning

confidence: 94%

Disconnected submarine lobes as a record of stepped slope evolution over multiple sea-level cycles

et al. 2018

Self Cite

View full text Add to dashboard Cite

The effects of abrupt changes in slope angle and orientation on turbidity current behavior have been investigated in numerous physical and numerical experiments and examined in outcrop, subsurface, and modern systems. However, the long-term impact of subtle and evolving seabed topography on the stratigraphic architecture of deep-water systems requires fine-scale observations and extensive 3-D constraints. This study focuses on the Permian Laingsburg and Fort Brown formations, where multiple large sand-rich systems (Units A-F) have been mapped from entrenched slope valleys, through channel-levee systems, to basin-floor lobe complexes over a 2500 km 2 area. Here, we investigate three thinner (typically <5 m in thickness) and less extensive sand-rich packages, Units A/B, B/C, and D/E, between the large-scale systems. Typically, these sand-rich units are sharp-based and topped, and contain scours and mudstone clast conglomerates that indicate deposition from high-energy turbidity currents. The mapped thickness and facies distribution suggest a lobate form. These distinctive units were deposited in similar spatial positions within the basin-fill and suggest similar accommodation patterns on the slope and basin floor prior to the larger systems (B, C, and E). Stratigraphically, these thin units represent the first sand deposition following major periods of shut-down in sediment supply, and are interpreted as marking a partial re-establishment of sand delivery pathways creating "disconnected lobes" that are fed mainly by flows sourced from failures on the shelf and upper slope rather than major feeder channel-levee systems.Thickness and facies patterns throughout the deep-water stratigraphy suggest seabed topography was present early in the basin formation and maintained persistently in a similar area to ultimately form a stepped slope profile. The stepped slope profile evolved through three key stages of development: Phase 1, where sediment supply exceeds deformation rate (likely caused by differential subsidence); Phase 2, where sediment supply is on average equal to deformation rate; and Phase 3, where deformation rate outpaces sediment supply. This study demonstrates that smaller systems are a sensitive record of evolving seabed topography and they can consequently be used to recreate more accurate paleotopographic profiles.

show abstract

“…Deep erosion surfaces overlain by palaeosols are interpreted to occur as a result of relative base-level fall, F I G U R E 6 Representative bottomset logs from Localities L.X and L.VIII ( Figures 2C and 4) in Melissia Valley (FA 4a). As such, sequence boundaries can either be masked or simply misinterpreted-a common problem in deep water successions (Covault and Graham, 2010;Hodgson et al, 2016). The sandstone-mudstone content is variable between them.…”

Section: Key Stratal Surface Interpretationmentioning

confidence: 99%

Syn‐rift delta interfan successions: Archives of sedimentation and basin evolution

Barrett

Gawthorpe

Collier

et al. 2019

The Depositional Record

Self Cite

View full text Add to dashboard Cite

Models that aim to capture the interactions between sediment supply, base level and tectonism recorded in fan delta successions in rift basins have not considered the stratigraphic archive preserved in interfan areas; yet interfan stratigraphy can provide a complementary record to the fan delta axes. The exhumed Early-Middle Pleistocene Kerinitis and Selinous fan deltas, in the hangingwall of the Pyrgaki-Mamoussia (P-M) Fault, Corinth Rift, Greece, offer an ideal laboratory for the assessment of interfan architecture. Furthermore, using the geometry of adjacent present-day fan deltas, interfans are classified into three end-members. The classification is based on their lateral separation, which determines the degree of interfingering of topset, foreset and bottomset deposits. Qualitative (facies, stratal geometries, nature of key surfaces) and quantitative (stratigraphic thickness, bedding dip, palaeocurrents, breakpoint trajectories) data were collected in the field and from unmanned aerial vehicle photogrammetry-based 3D outcrop models of the exhumed fan delta successions. The ancient Kerinitis-Selinous interfan architectures record: (a) initial westward progradation of the Kerinitis fan delta into the interfan area (Phase 1), (b) subsequent progradation of the Selinous fan delta into the interfan area and asymmetric growth of both fan deltas eastward (Phase 2), (c) stratal interfingering of foresets from both systems (Phase 3), and (d) relative base-level fall, erosion and reworking of sediments into the interfan area (Phases 4 and 5). The Kerinitis-Selinous interfan evolution is linked to initial net subsidence of the P-M Fault (Phases 1-3) and subsequent net uplift (Phases 4 and 5) resulting from a northward shift in fault activity. Theinterfan area provides a more complete stratigraphic record than the proximal axial areas of the fan deltas of the early stages of basin uplift, through higher preservation potential and protracted submergence. Therefore, for the most comprehensive insight into basin evolution, interfan analysis should be undertaken in concert with analysis of the fan delta axes. K E Y W O R D SBasin evolution, fan delta, interfan, stratigraphy, syn-rift. |

show abstract

Time-Transgressive Confinement On the Slope and the Progradation of Basin-Floor Fans: Implications For the Sequence Stratigraphy of Deep-Water Deposits

Cited by 91 publications

References 104 publications

Frontal and Lateral Submarine Lobe Fringes: Comparing Sedimentary Facies, Architecture and Flow Processes

Frontal and Lateral Submarine Lobe Fringes: Comparing Sedimentary Facies, Architecture and Flow Processes

Disconnected submarine lobes as a record of stepped slope evolution over multiple sea-level cycles

Syn‐rift delta interfan successions: Archives of sedimentation and basin evolution

Contact Info

Product

Resources

About