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Depositional Control on Hydrocarbon Accumulations in Deepwater Nigeria*
By
Xijin (CJ) Liu1
Search and Discovery Article #40226 (2006)
Posted December 12, 2006
*Adapted from extended abstract prepared for presentation at AAPG Annual Convention, Houston, Texas, April 9-12, 2006
1West Africa Exploration, ConocoPhillips, Houston, TX 77079 ([email protected])
Introduction
Seafloor geomorphology controls deepwater sand deposition that, combined with structural configurations, controls hydrocarbon accumulation. Structural control of hydrocarbon accumulations is very well known, but depositional control seems to be very important in some deepwater exploration areas. This is demonstrated by a case study on Nigeria deepwater discoveries.
Many discoveries have been made in anticlinal structures in the Nigeria deepwater. The anticlines are located from the shale-diapir province, through the inner thrust belt and translational province, to the outer toe-thrust belt. One of the most interesting observations is that most of the discoveries were made on the downslope (basinward) side of the anticlines.
Two possible explanations, among others, become obvious. One is that sand deposition preferentially occurs on the downslope side of the structures at the time of deposition synchronous with structural growth (generated by shale diapirism or thrusting). This is the result of relatively greater accommodation space and/or hydraulic jump of turbidity current flow across seafloor topographic highs. The second one is that hydrocarbon migration and charge preferentially occur, along a regional depositional slope, in an updip (landward) direction. This extended abstract is aimed to expand the discussion of the two explanations.
Examples of hydrocarbon discoveries in the deepwater Nigeria on the downslope side of anticlinal structures (shale-cored diapirs or thrust-generated anticlines) include Bonga, Bonga Southwest, Akpo, Uge, N’Golo, and Obo North. A common characteristic of all the structures is that reservoir sand deposition was synchronous with structural growth. The structures occurred as seafloor topographic highs during the time of sand deposition. Turbidite elements of the reservoir sands consist primarily of channel fill and associated frontal splays (e.g., lobate sheet sands).
There are other discoveries, such as Agbami, in the deepwater Nigeria, which do not exhibit this pattern. A detailed examination of those discoveries reveals that the reservoir sands were deposited prior to structural growth, and therefore the structures did not affect sand distribution. Moreover, turbidite elements of the reservoir are mainly basinal-plain terminal sheet-sand lobes.
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Depositional Control on Sand DistributionDeepwater gravity sedimentation in general and sand deposition in particular is greatly influenced by seafloor topography with sediment being largely focused into topographic lows. On a continental slope, sedimentation of turbidite and associated gravity flow deposits are controlled by local base level and accommodation space which, in turn, is controlled by the slope equilibrium profile (Pirmez, 2000; Prather, 2003). Erosion/incision occurs in areas above the profile, and deposition occurs in areas below the profile. Growth of shale-core diapirs, due to either deep-seated duplexing/thrusting as a result of downslope gravity gliding along detachment surfaces or differential sediment loading, generate subtle seafloor topographic highs, thus leading the depositional surface to deviate from the equilibrium profile and creating local areas of erosion and accommodation space for deposition. Pre-existing or syn-growth channels along the continental slope across these seafloor highs have to adjust themselves. Channel thalwegs will be subject to either down-cutting (deepening) and possible headward erosion across these highs (if thalweg elevation is above the equilibrium profile) or aggradation (shoaling) on the downslope flank of the highs and the adjacent structural low area (where thalweg is beneath the equilibrium profile).
Turbidity current flows emanating down from a seafloor topographic high
is forced to undergo a hydraulic jump from a Froude-supercritical flow
regime to a highly Froude-subcritical regime. This results in a deep,
placid, slow-moving turbidity current farther downstream (Parker, 2003),
leading to deposition of sands that cannot be carried farther
downstream. Skaloud and Cassidy (1998) used the hydraulic jump theory to
explain the sand deposition on the downslope flanks of both Bonga and
N’golo It is possible that sands can be carried by a single turbidity current across multiple structural highs and deposit them in the form of terminal lobe if the channel thalweg is more or less close to the equilibrium profile and flow thickness is less than the channel depth. During periods of active structural growth, such equilibrium condition will be disrupted and sand deposition should occur, although non-uniformly, across different channel segments across multiple structures. A modern example is shown in Figure 2.
Sands are expected to be predominantly deposited on the downslope sides
of structural highs due to a greater accommodation space (below the
regional depositional equilibrium profile). Hydraulic jump of turbidity
current flows emanating down from these structural highs is the dominant
hydrodynamic process for sand deposition. The upslope flank of the
structural high as manifested by the channel thalweg profile is
generally above the equilibrium profile. Consequently, little sand will
be deposited there and on the top of the highs, assuming turbidity
current flow thickness is less than the channel depth. Even if sands are
deposited across the top and upslope flanks of the highs during periods
when structural growth rate is far less than sedimentation rate across
the entire channel stretch, they may not be well preserved because
subsequent structural growth and turbidity current flows may lead to
erosion. For thick sand deposition within a particular channel segment
downslope of a structural high, it requires a greater accommodation
space and higher preservation potential, other factors being equal. This
can occur when structural growth rate is significantly greater than the
background sedimentation rate, such that a high topographic relief of
the seafloor is created. This could create a ponded mini-basin upslope
of the structural high, where sands could be deposited (Prather, 2003).
Once the mini-basin is filled to such a level that the thalweg elevation
plus a presumed turbidity current flow thickness exceeds the elevation
of the regional equilibrium profile, sand will start to be funneled down
the structural high into the downslope part of the channel and be
potentially deposited in the next basinward mini-basin. This will be the
time for relatively thick sand deposition, until the downslope
mini-basin is filled. Therefore, the timing of thick sand deposition in
a slope
The overall succession of the sand package generally exhibits a
thinning-upward trend (Figure 3). If
sedimentation rate keeps up with structural growth and no significant
accommodation space is available along the channel stretch, only thin
but possibly more sands will be deposited due to a less degree of
amalgamation. It is also possible that more unconfined lobate-shaped
sandbodies will be deposited due to relatively shallow thalweg depth and
ease of overbank flow stripping. It is clear from the above discussion
that the downslope flanks of shale-cored structural highs are loci for
sand deposition as long as structural growth continues and sedimentation
rate is not high enough to smooth out its seafloor topographic relief.
The thickness and number of sands are dependent upon, other factors
being equal, the relative rate between structural growth and
sedimentation. High rate of structural growth creates more opportunities
for thick sand deposition on the downslope flank of the
Hydrocarbon Migration/Charge
In addition to the depositional control over hydrocarbon accumulation
pattern, it is also important to note that hydrocarbon migration and
charge also play a critical role. Two most important factors are worthy
of consideration. First, hydrocarbon migration from source-rock kitchen
generally occurs in an updip direction. Secondly, the fetch area from
source-rock kitchen is generally much greater for its updip shale-cored
anticlinal structures than that for its downdip structures (Figure
4). Therefore, charge volume for a given
Comment
The finding of the hydrocarbon accumulation pattern in the deepwater
Nigeria can potentially be applied to other deepwater exploration
regions such as the Gulf of Mexico and offshore Angola, where the target
stratigraphic intervals were deposited synchronously with or shortly
after structural growth. However, it does not apply to the stratigraphic
intervals or areas where sand deposition was not affected by structural
growth (e.g., a basin-floor fan
Conclusions1.Several hydrocarbon discoveries in deepwater Nigeria suggest that hydrocarbon accumulations preferentially occur on the downslope flank of shale-cored structural highs. 2.The hydrocarbon accumulation pattern is primarily controlled by preferential sand deposition on the downslope sides of the structures. 3.Hydrocarbon migration direction and charge volume may also play an important role for the observed hydrocarbon accumulation pattern. 4.The finding of hydrocarbon accumulation pattern can be applied to other deepwater basins where structural growth is synchronous with sand deposition.
References
Chapin, M., P. Swinburn, R. Van der Weiden, D. Skaloud,
S. Adesanya, D. Stevens, C. Varley, and J. Wilkie, 2002, Integrated
seismic and subsurface characterization of Bonga Pirmez, Carlos, R.T. Beaubouef, and S.J. Friedmann, 2000, Equilibrium Profile and Baselevel in Submarine Channels: Examples from Late Pleistocene systems and Implications for the Architecture of Deepwater Reservoirs, abstract, in GCSSEPM 20th Annual Bob F. Perkins Research Conference, 2000, Houston, TX. Prather, B.E., 2003, Controls on reservoir distribution, architecture and stratigraphic trapping in slope settings: Marine and Petroleum Geology, v. 20, p. 529-545. Skaloud, Dieter K., and Phillip Cassidy, 1998, Exploration of the Bonga and Ngolo Features in Deepwater Nigeria (abs.): AAPG Bulletin, v. 82, p.1883-1984. Toniolo and Parker, 2003, Depositional turbidity currents in diapiric minibasins on the continental slope: Theory, experiments, and numerical simulation, extended abstract for presentation at the AAPG Annual Meeting, Salt Lake City, Utah, May 11-14, 2003.
AcknowledgmentThe author is very grateful for instructive discussion with and input from the Deepwater Nigeria Exploration Team of ConocoPhillips. I thank Dave McGee and Frank Snyder who provided very good technical editing. The author is also thankful for ConocoPhillips management and coventures for approval to publish this material. |
