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Journal of Sedimentary Research, 2007, v. 77, 225–238

Research Article

DOI: 10.2110/jsr.2007.024

THREE-DIMENSIONAL SEISMIC ARCHITECTURE OF FLUVIAL SEQUENCES ON THE LOW-GRADIENTSUNDA SHELF, OFFSHORE INDONESIA

Y. DARMADI,* B.J. WILLIS,{ AND S.L. DOROBEK1

Department of Geology and Geophysics, Texas A&M University, College Station, Texas 77845-3115, U.S.A.

ABSTRACT: The sequence stratigraphy of fluvial–deltaic strata deposited near the center of the wide, gradually subsidingSunda Shelf differs from standard highstand examples because low accommodation and low depositional gradients restrictedthe thickness of fluvial–deltaic sequences and the depth of lowstand fluvial incision. In this setting sea-level fluctuations mayhave had less influence on fluvial depositional patterns, and fluvial stratigraphy is more likely to be defined by changes in riverdischarge during gradual aggradation. The upper Muda Formation in West Natuna Basin, offshore Indonesia, is a 225-m-thick,dominantly fluvial succession that prograded onto the middle part of the Sunda shelf from Pliocene to Holocene. The succession

changes upward from offshore shelf deposits, through a thin interval of deltaic deposits, a succession of fluvial deposits, andfinally a thin transgressive succession directly beneath the modern sea floor.A high-resolution seismic survey (17 km by 40 km in area) of Belida Field near the middle of the Sunda shelf provides

exceptional images of changing fluvial architecture within five erosionally based, fluvial sequences. Sequences, each several tensof meters thick, are characterized by low-relief basal incisions that extend laterally onto interfluves cut by a network of gullies.Although a regressive stacking pattern of successive sequences is defined to some extent by an increase in the relief of basalerosion and a decrease in average sequence thickness, it is best defined by progressive increase in the extent of gully formationonto interfluve areas (indicating longer periods of interfluve exposure).

Channel size tends to decrease upward within individual sequences, recording both a decrease in the size of the largestchannels and greater preservation of smaller tributary and floodplain drainage channels. The largest channels preserved directlyabove the better developed sequence boundaries tend to be more sinuous and to have more extensive inner-bend accretiondeposits than those that cut down from horizons higher within sequences. This suggests that incised channels had more streampower to erode their banks relative to the sediment loads they carried. Although mechanisms controlling the episodic shallowincision and then aggradation of these fluvial systems are difficult to constrain from variations observed in this small study area,

the consistent thickness of the Muda Formation observed in regional 2D seismic sections is evidence against significantsyndepositional tectonic deformation or differential subsidence. Low regional gradients and great distance of the study areafrom the paleo-shelf edge (, 1000 km) are evidence against direct sea-level influence. Larger channel sizes directly abovesequence boundaries supports temporal changes in channel discharge, perhaps related to climatic changes within the drainagebasin. Recognition of episodic channel incision and bypass alternating with periods of floodplain aggradation influencespredictions of channel-deposit connectivity based on channel proportion.

INTRODUCTION

Vertical changes in channel patterns within fluvial successions have

been widely inferred in sequence stratigraphic models of fluvial systems.

Stratigraphic predictions are generally based on alluvial architecture

models (Leeder 1978; Allen 1978; Bridge and Leeder 1979), combinedwith ideas about changes in sediment aggradation rates of nearshore

sediments during changes in sea level (Shanley and McCabe 1991, 1993;

Wright and Marriott 1993; Plint et al 2001; Olsen et al 1995; Legarreta

and Uliana 1998; Posamentier 2001; see also recent review in Blum andTornqvist 2000). These models generally predict that fluvial gradientssteepen and floodplain widths decrease as aggradation slows and river

channels incise during sea-level fall, leading to preferential preservation of channel deposits relative to overbank deposits and braided channelpatterns. Sea-level rise is predicted to decrease fluvial gradients and widen

floodplains as sediments aggrade and river incisions fill, leading to greaterpreservation of floodplain deposits and meandering channel patterns.

Based on these general ideas, sandier fluvial successions have commonlybeen interpreted as deposits of braided river systems, and muddier fluvialsuccessions as deposits of meandering river systems.

Studies of fluvial architecture in outcrop typically provide only isolatedtwo-dimensional views of fluvial architecture. Although vertical varia-tions in the proportion of channel to overbank deposits over tens to

hundreds of meters are commonly observed, few examples have adequateage control to constrain changes in aggradation rate associated with

* Present address: ConocoPhillips Indonesia, Gatot Subroto, Jakarta 12930,

Indonesia

{ Present address: Chevron Energy Technology Company, 1500 Louisiana

Street, Houston, Texas 77002, U.S.A.

1 Present address: Maersk Oil and Gas, Esplanaden 50, 1263 Copenhagen K,

Denmark

Copyright E 2007, SEPM (Society for Sedimentary Geology) 1527-1404/07/077-225/$03.00



observed upsection changes in the proportion of channel deposits. It is

also generally difficult to define changes in channel pattern from vertical

cross sections (Bridge 1985). The result is that most stratigraphic studiesof ancient fluvial deposits are strongly inferential with regards to links

between channel-deposit abundance, aggradation rate, and channel

pattern and few studies provide robust tests of these ideas.

Recent studies of Quaternary fluvial systems that have been extensively

cored anddated (e.g.,Blum 1993;Tornqvist 1993; Blum et al 1996; Tebbens

et al. 1999; Tornqvist et al. 2000; Blum and Tornqvist 2000) are beginning

to provide a more complex picture of controls on fluvial architecture.

Variations in sea level and climate are better known for these younger time

intervals, and thus extrabasinal controlling factors are better constrained.

In some cases, these studies have also documented temporal changes in

channel patterns based on examination of abandoned river courses or

preserved terraces (e.g., Starkel 1991; Blum et al. 1995; Aslan and Autin

1999). One important insight from Quaternary studies is that climatic

changes that affect fluvial water and sediment discharge are probably as

important as sea-level variations in defining alluvial architecture. For

example, Blum and Lancaster (2005) showed that deepest incision of the

Mississippi valley occurred during the beginning of eustatic sea-level rise as

melting continental glaciers within the drainage basin significantly

increased high river discharges. Khadkikar and Rajshekhar (2005)

indicated that rivers incised along the western coast of India during the

most recent period of eustatic sea-level rise due toincreased river discharges

related to intensification of monsoon rainfall. A limitation of Quaternary

stratigraphic studies is that for the most part they give insight only into

fluvial–deltaic response to the very rapid sea-level changes that characterize

the last eustatic cycle, and that changes in fluvial architecture are defined

only by isolated cores and river cutbank exposures (rare exceptions to the

latter include the unprecedented coring studies of the Rhine–Meuse delta,

summarized in Berendsen and Stouthamer 2001).Improvements in 3D seismic acquisition and processing show promise in

providing new views of changing alluvial architecture. Although 3D seismic

records do not show the details of facies variations that can be documented

in large outcrops, nor are they constrained by the resolution of dating

achieved in some studies of Quaternary deposits, they have vertical and

lateral extent and continuity that is far beyond that which can be obtained

using other methods. Most importantly for analysis of alluvial architectural

models, 3D seismic volumes can be used to link records of vertical changes

in channel-deposit abundance and incision depth with planview changes in

channel-deposit width, distribution, and pattern. The few published studies

of fluvial deposits documented by modern 3D seismic data show

magnificent views of complex channel-body geometries and floodplain

features imaged in horizontal time slices (e.g., Burnett 1996; Carter 2003;

Posamentier 2001; Miall 2002; Zeng and Hentz 2004). Additional studies

are needed that better link vertical variations with planview changes of

fluvial deposits before the full potential of these new data in assessing

alluvial architecture models will be realized.

This study is based on a 3D seismic survey of Belida field in the West

Natuna Basin, South China Sea (Fig. 1). The focus is on the Pliocene to

Holocene river-dominated, upper Muda Formation, which contains

fluvial features that are well imaged in this seismic volume. The goal of

this study is to relate stratigraphic variations defined by vertical changes

in channel size and abundance with planview changes in the distribution

and pattern of observed channel bodies and evaluate possible factors that

may have caused these changes.

FIG. 1.—Ancient drainage patterns across thesouthwestern South China Sea (Sunda shelf) thatformed during the Last Glacial Maximum andpossibly also during older Quaternary eustaticlowstands (after Pelejero et al. 1999). Map showsshallow shelf areas exposed during lowstands

and major paleo-drainage systems that can beidentified by present-day seafloor bathymetry(Molengraaff 1921; Tjia 1980). Belida Field,located in the broad shallow southwestern partof the South China Sea, is nearly 1000 kilometersaway from the continental shelf edge and a fewhundred kilometers basinward of the modernshoreline. Inset map of the study area showsintersection of each 200th north–south cross-lineand east–west inline seismic traces (dots), loca-tion of the seismic cross section in Figure 3(dashed line A–A9), and the outline of the areashown in Figures 4 and 5.

226 B.J. WILLIS ET AL. J S R



GEOLOGIC SETTING

The West Natuna Basin consists of a series of small, roughly east–west

oriented depocenters with intervening basement ridges that formed

during Paleogene rifting across the southern South China Sea (‘‘Sunda

shelf’’) region (Fig. 1; White and Wing 1978; Wongsosantiko and

Wirojudo 1984; Daines 1985; Ginger et al. 1993; Murray 2003). Many

half-graben depocenters of the West Natuna Basin experienced significant

contraction during late Oligocene to Miocene time, which formed the

‘‘Sunda Folds,’’ classical examples of inverted basins (Ginger et al. 1993;

Olson and Dorobek 2000). The Upper Miocene to Recent Muda

Formation, about 600–750 m thick, is a broadly recognized lithostrati-

graphic unit in the West Natuna Basin that formed during a period of slow regional subsidence after inversion had ended around 10 Ma

(Ginger et al. 1993; Phillips et al. 1997; Madon and Watts 1998; McClay

and Bonora 1998; Murray 2003). Thus, strata of the Muda Formation are

largely undeformed.

The Muda Formation is defined at its base by a thick interval of outer-

shelf mudstone facies that generally define the topseal for underlying

sandstone and carbonate reservoirs in many basins across the Sunda shelf

(Mattes 1979; Cossey et al. 1982; Sutoto 1991; Mayall et al. 1995; Michael

and Adrian 1996; Matthews et al. 1997; Maynard and Murray, 2003). The

Muda Formation was generally thought to consist entirely of marine

mudstones before the 1990s, because well logs and drill cuttings were

rarely collected until deeper hydrocarbon-bearing intervals were pene-

trated. Recent studies have combined high-resolution seismic data and

shallow sediment cores to document variations within the upper 50–

100 m of the Muda Formation and its lateral stratigraphic equivalents.

These studies demonstrated that shallow intervals of the Muda

Formation consist of deposits that formed during the last sea-level cycle,

including: (1) fluvial channels deposited during the Last Glacial

Maximum lowstand, (2) transgressive deposits formed during the post-

Pleistocene sea-level rise, and (3) shallow-shelf deposits formed during the

present-day highstand (e.g., Aleva 1973; Batchelor 1979; Emmel and

Curray 1982; Evans et al. 1995; Hanebuth and Statteger 2003; Wong et al.

2003). Deeper intervals of the Muda Formation remain poorly

documented.

Belida field, in the western part of West Natuna Basin (Maynard et al.

2003), is in the center of the Sunda shelf, nearly 1000 km up dip (west) of

the modern shelf slope break. Currently in 56 m deep water, this area is

likely to have been subaerially exposed during Pliocene to Holocene

maximum glacio-eustatic lowstands (Fig. 1). Undeformed post-inversion

strata in Belida field (Fig. 2), including the uppermost Arang Formation

and the overlying Muda Formation, can be divided into three intervals.

Seismically, each of these intervals is defined by strata with channel-form

reflections that are separated by strata with more-continuous horizontal

FIG. 2.—Seismic cross section and chronostratigraphy of Belida Field, West Natuna Basin (after Palynova 2003). Hydrocarbon reservoirs are found within invertedhalf-graben structures (below 750 ms twtt). The Muda Formation, formed during approximately the last 10 Myr, was deposited after tectonic inversion had ended andthe region gradually subsided. The base of the Muda Formation is defined by an abrupt fining to shale, above an interval of channels in the uppermost Arang Formation.This study addresses an interval with increasing channels in the upper 500 ms twtt of this seismic record.

MUDA FORMATION THREE-DIMENSIONAL FLUVIAL ARCHITECTURE 227J S R



reflections. Each interval is estimated to record several million years of

deposition, on the basis of proprietary biostratigraphic data from a well

in an adjacent area of the West Natuna Basin (Darmadi 2005) and by

comparisons with Morley et al. (2003). The oldest of these intervals

include channel-form reflections and overlying parallel-horizontal reflec-

tions in the upper Arang Formation that may have been mildly influenced

by the last stages of basin inversion. The second interval is defined by

channel-form reflections within the uppermost Arang Formation and

parallel-horizontal reflections in the basal part of the Muda Formation.The third interval includes channel-form reflections in the upper part of

the Muda Formation and overlying parallel-horizontal reflections that

directly underlie the modern sea floor. Each of these intervals are

interpreted to be third-order stratigraphic sequences (i.e., have durations

of a few million years). Their boundaries, however, do not necessarily

record an abrupt coarsening across a single discrete allostratigraphic

surface (in contrast to the definition of Van Wagoner et al. 1987), but

rather appear to be characterized by a gradual upward change in facies

across a succession of smaller-scale internal unconformity-bounded

intervals. This study focuses on smaller-scale vertical variations within

the youngest of these third-order stratigraphic intervals.

METHODS

A 3D seismic-reflection survey acquired in 2001 by Conoco Indonesia

across the 17 km by 40 km area of Belida field has in-line spacing of 25 m

and cross-line spacing of 12.5 m. Because most wells in Belida field

include information only from deeper stratigraphic levels where

petroleum reservoirs are located (i.e., Eocene to upper Miocene strata),

the thickness of Muda deposits was estimated by a comparison of vertical

seismic variations to velocity logs that extend through the shallow part of

four wells in Belida field. Given the relatively shallow depth of the Muda

Formation, average seismic velocity is estimated to be 1650 meters per

second. The highest frequencies recorded in the seismic data are nearly

100 Hz (dominant frequencies ranged from 50 to 60 Hz), potentially

allowing stratal features less than 10 m thick to be resolved. Seismic

mapping was accomplished using combined in-line and cross-line vertical

seismic sections and horizontal time slices of successive 4 ms twtt

(milliseconds two-way travel time) thick horizons.Seismic root-mean-squared amplitude variations were used to interpret

depositional features and geomorphologic patterns in time slices.

Interpretation of stratigraphic trends defined by vertical changes of the

fluvial architecture was a challenge because channel deposits of different

size and incision depth that are cut down from a variety of horizons are

superimposed within individual seismic slices. By scrolling through

successive horizontal time slices and vertical seismic cross sections

simultaneously, individual channel-form reflections were assigned to the

stratigraphic horizon from which they incised. Although many channel

bodies where so highly fragmented by incision of subsequent channels

that it was difficult to define their dimensions, where bodies were more

complete, their width, depth, and sinuosity were recorded relative to their

incision horizon. Planview maps of these more complete channels were

compiled for successive stratigraphic intervals to show vertical changes inchannel size, direction, and fluvial style.

Seismic Variations within the Upper Muda Formation

A seismic section of the upper 500 ms twtt interval of Belida field

(Fig. 3) shows the location and cross-sectional geometry of channels in

the upper part of the Muda Formation. This seismic cross section extends

from a high-amplitude, laterally continuous horizontal reflection in the

Muda Formation at 430 ms twtt upward to the modern sea floor at 56 ms

twtt, this represents a thickness of about 225 m. Channels imaged within

this interval become more abundant and on average larger upsection.

Larger channels appear to cut downward preferentially from particularhorizons, an observation that was used to subdivide this interval intoa succession of thinner sequences. Boundaries of these thinner sequenceswere defined by tracing particular reflections across the seismic volume

that marks the base of clusters of more deeply incised channels. Althougheach sequence boundary is defined by a reflection that is continuousacross the seismic volume, the basal surface of the oldest sequence(Sequence Boundary 1 or SB 1) is less clearly an allostratigraphic surface

(versus a clustering of channel deposits cut down from slightly differenthorizons) than those that define the four younger sequences. Theyoungest two sequences (above SB 4 and SB 5) are complexly nestedwithin the same interval, and the boundary separating these sequences(SB 5) could be defined only locally because the associated interfluves

merge within seismic resolution with those of SB4. Individual sequencesare 50 to 100 ms twtt (about 30–60 m) thick and are interpreted to

represent deposition over about 0.5 Myr on the basis of simpleinterpolation of the estimated age range of the entire Muda Formation.Amplitude variations across representative horizontal seismic time slicesthrough this interval (Fig. 4) are discussed in detail below. Becausechannels incised from different sequences are commonly superimposedwithin horizontal time slices, maps of channel bodies incised froma specific stratigraphic interval are presented for a similar set of intervalsas shown in each of the presented seismic slices (Fig. 5).

Below Sequence 1

Reflections in the basal part of the seismic cross section (Fig. 3;between 500 and 400 ms twtt) are laterally continuous and subhorizontal.Lateral variations in amplitude observed in horizontal seismic time slicesthrough this interval are broad and gradual over 5 to 10 km. Above400 ms twtt, sparse small channels are defined by high-amplitudereflections, each less than 100 meters wide, 10–20 ms twtt (, 6–12 m)deep, and about 2 km in channel-bend wavelength (Fig. 4A). Thesechannels are generally oriented southwest–northeast and are locallyhighly sinuous (i.e., ratio of channel-centerline to straight-line distance of 2.5–3.5). Bar accretion deposits, visible on the insides of some channel-

bend segments, indicate migration dominated by expansion. The fewchannel bends with asymmetric accretion patterns (Figs. 4A, 5A) suggestpaleoflow to the northeast. Although interchannel amplitude variationsare more variable upsection, they remain gradual over a few kilometersand locally appear to be lobate in planview (Fig. 4A). Two largerchannels defined by low-amplitude reflections, on the order of a kilometerwide and nearly 45 ms (, 25 m) deep, cut down from horizons just belowSequence Boundary 1 (400–430 ms twtt). These larger channels are nearlysymmetrical in cross section, have low sinuosity, and lack evidence of

bank accretion deposits. Smaller, higher-sinuosity channels, like thoselower within this interval, are also observed.

Sequence 1

Sequence 1 (generally between 350 to 250 ms twtt; on average about60 m thick) is underlain by Sequence Boundary 1. Basal deposits are low-to moderate-sinuosity channel deposits up to 2 kilometers wide and50 ms twtt (, 30 m) deep (Figs. 3, 4B). The sequence boundary is

defined by laterally mapping a reflection cut by the most deeply incised of these channels through the entire seismic volume (Fig. 6A). Although this

boundary delineates an interval along which larger channels areconcentrated (Fig. 3), it cannot be claimed conclusively that it representsa higher-order allostratigraphic surface relative to those that extendlaterally away from similar-scale channels found slightly lower and higherwithin the stratigraphy. The channel used to define this sequenceboundary shallows and thins toward the northeast (Fig. 6A), a directionthat can be inferred to be downstream on the bases of accretion depositsin adjacent channels.




Upward into the middle of this sequence, large channels gradually

become more sinuous (Figs. 4B, 5B) and smaller channels become moreabundant (cf. Fig. 5B). The larger channels are about 1.5 km wide and

35 ms twtt (, 20 m) deep, and have wavelengths averaging 5 km. In timeslices, amplitude variations between channels are pronounced and

complex, changing laterally over a few kilometers. Although in several

locations, small channels appear to pass laterally into more diffusekilometer-wide lobate zones defined by higher-amplitude variations, the

complex distribution and limited resolution of small channel segmentsmakes it difficult to demonstrate this link conclusively. Channels in the

FIG. 3.— A) Uninterpreted and B) interpreted seismic cross section of the upper Muda Formation (upper 500 ms twtt). See inset map in Figure 1 for location of crosssection. Interpretations are based on examination of this and adjacent cross sections and horizontal time slices spaced each 4 ms twtt upward within the seismic volume.




FIG. 4.—Selected horizontal time slices showing the distribution and geometry of seismic-amplitude variations in different horizons of the upper Muda Formation atBelida Field. A) Horizon below Sequence Boundary 1 shows small meandering channels (arrows point to a few specific examples) that cross an area characterized by

broad, gradual amplitude variations. B) Larger channels with moderate to high sinuosity dominate horizons in the middle interval of Sequence 1 (arrows point to twoexamples). C) Channels with widely varying dimensions observed in the upper interval of Sequence 1. The largest channels have fairly straight, south–north orientation(arrows point to two examples). D) Horizon near the top of the incision fill above Sequence Boundary 2 (area of deepest underlying incision is marked by the dashed line(i ). Areas adjacent to this incision show local dendritic gully formation (arrow ii ). E) Large channel with well imaged bar accretionary deposits accumulated in the area of deepest incision along Sequence Boundary 3 (arrow i ). The very base of Sequence Boundary 4 incision also intersects this time slice (arrow ii ). Small channels that cutdownward from within the upper part of Sequence 2 (arrow iii ) vary in sinuosity and pattern. Larger channels that cut down from the upper part of Sequence 3 are allfairly straight (arrow iv). F) Time slice intersecting the upper part of the basal channel along Sequence Boundary 3 (arrow i ) shows gully formation into adjacentfloodplain areas (arrow ii ). Straighter large channels in the upper part of Sequence 3 also penetrate this horizon (arrow iii ). Inner-bank bar accretion in the basal channelof Sequence 4 is also observed (arrow iv). G) Incised channels cut down from Sequences 4 and 5 into nearly the same interval. The largest channels incised from bothsequences contain well imaged inner-bank bar accretion deposits (arrow i points to bar in a Sequence 4 channel, and arrow ii points to bar in a Sequence 5 channel).Narrower channels with adjacent dendritic gullies cut down from Sequence 4. Straighter channels without adjacent dendritic gullies cut down from higher intervals withinSequence 4. H) Channels with adjacent dendritic gullies (i ) decrease in abundance and average size and increase in sinuosity from northwest to southeast in the upper partof Sequences 4 and 5. A smaller sinuous channel in the upper part of Sequence 5 ( ii ) has adjacent dendritic gullies that overlie deposits of Sequence 4.




upper part of Sequence 1 are uniformly smaller (less than a kilometerwide and 10 ms twtt deep) and have low sinuosity (Figs. 3, 4C, 5C). On

average they are more uniformly south-to-north oriented than thoselower in the sequence. Interchannel amplitude variations in time slicesalso are more subdued than those below Sequence Boundary 1.

Sequence 2

Sequence 2 (generally between 250 to 170 ms twtt; on average about50 m thick) is defined at its base by a reflection with nearly 90 ms twtt(, 55 m) of relief (Fig. 6B). The dominant incision along this sequenceboundary is a nearly two kilometers wide, 60 ms twtt (, 40 m) deep,north–south oriented, straight channel. Reflections in this channel areinitially concordant with its base, and then they successively become more

horizontal. Several smaller channels that also cut into this basal surface(Figs. 4D, 5D) are generally parallel to the larger channel, and togetherdefine a nearly 10-km-wide incision trend (Fig. 6B). In one location, smalldendritic gullies expand over a few kilometers onto the adjacent interfluve

adjacent to this incised trend (Fig. 4D).

Above the interval of incision, isolated larger channels (kilometers

wide) have a fairly straight north–south orientation. In the upper part of this sequence narrower channels have progressively more west-to-easttrends and have more variable planform geometry, ranging from higher

sinuosity to straighter segments with downstream branching or anasto-mosing geometries (Fig. 4E, F). Smaller channels are defined bycontrasting amplitude variations (i.e., some have higher amplitudes andothers lower amplitudes than surrounding deposits). The complex

distribution of smaller channel segments, many of which are near thelimit of seismic resolution, makes it difficult to define patterns of amplitude variation within strata between channel bodies.

Sequence 3

Sequence 3 (generally between 170 to 120 ms twtt, on average about30 m thick) is defined at its base by a sequence boundary with slightlyover 50 ms twtt (, 30 m) of relief (Fig. 5C). The stratigraphically lowest

parts of this sequence boundary define a sinuous, west–east incised trend,in contrast to the south–north trend of incisions that characterizeunderlying sequence boundaries. A large sinuous channel with well-

imaged bar accretion deposits is found in the deepest part of the mainincision along Sequence Boundary 3 (Fig. 4E, F). The extent of theseaccretion surfaces and adjacent channel fill in cross section (Fig. 3), andplanview extent of bar accretion sets, indicate that this channel was nearly2 kilometers wide and 40 ms twtt (, 25 m) deep, and had a wavelength

of about 5–8 kilometers. Accretion sets extend more that four times thewidth of the adjacent channel fill, which has a sinuosity of about 3.Several similarly large channels, with more modest sinuosity, incise fromslightly higher stratigraphic levels into Sequence Boundary 3.

Time slices that cut through less incised areas along SequenceBoundary 3 show well developed dendritic gullies expanding severalkilometers away from the most deeply incised areas (Figs. 4F, 5F).Channels in Sequence 3, incised downward from above the horizon cut by

gullies, are less than a kilometer wide and 20 ms twtt (,

12 m) deep, andhave low sinuosity (Fig. 4F, G). Amplitude variations along thesechannel bodies suggest bar wavelengths of about 5 km, similar to thosein the high-sinuosity channel at the base of Sequence 3 (Fig. 5F).

Sequences 4 and 5

Sequences 4 and 5 (generally between 120 to 80 ms twtt, on average

about 25 m thick) are nested within nearly the same interval, and thustheir deposits are difficult to differentiate. The combined erosion surfaceat the base of these sequences has about 75 ms twtt (, 50 m) of relief.Both sequence boundaries rise locally to a distinctive horizon with

extensive dendritic gullies, some extending away from adjacent channels

onto interfluves over distances greater than 10 km. The distinctionbetween these two sequences is that gullies associated with incision of SB

5 locally erode into the tops of channels in Sequence 4. In contrast,

channels of Sequence 5 have gullies along their margins, but these gullies

do not extend across the main axes of these channel deposits.

The basal deposit of Sequence 4 is a moderately sinuous channel withwell imaged inner-bend bar accretion deposits (Figs. 4G, 5H). This

channel is 3 km wide and nearly 70 ms twtt (50 m) deep, and has a bendwavelength of 14 km. Asymmetry of accretion deposits in planview

suggests flow from northwest to southeast (Figs. 4 and 5, F and G). Otherlarge channel deposits that are cut into this interval are narrower,

straighter, a bit thinner (about 1 km wide and 30 ms twtt deep), and lack

obvious adjacent bar accretion deposits. Amplitude variations along one

of these straighter channels suggest that channel bars are about 3 km in

length (Fig. 4G). Crosscutting relationships suggest that these straighterchannels are younger in age than the large channel that floors the

sequence, even though they cut downward from nearly the same horizon.

The basal channel of Sequence 5, incised from nearly the same interval asthose in Sequence 4, has low sinuosity and bars with well imaged

accretion surfaces that suggest dominantly downstream migration from

west to east (Figs. 4G, 5G). There are distinct gullies along the margin of

this channel and along a narrower adjacent channel that crosses above thepath of the largest channel in Sequence 4.

Above the gullied surfaces of Sequences 4 and 5, channel segments with

varying size and sinuosity are generally discontinuous across horizontal

time slices. There is a decrease in channel size and abundance from west

to east across the study area. Strata are poorly imaged above this intervalbecause of the strength of the reflection from the modern ocean floor.

Interpretation of Depositional Patterns

The upper interval of the Muda Formation comprises an overall

progradational fluvial–deltaic succession formed on a broad, low-

gradient platform under conditions of relatively slow subsidence.Horizontal reflections near the base of the study interval (Figs. 2, 3;

400 to 700 ms twtt) image marine strata deposited during transgression

across the interval of fluvial channels in the lower Muda Formation(Fig. 2, from 700 to 900 ms twtt). The particularly high-amplitudereflection at about 430 ms twtt may be a maximum flooding surface.

Gradual amplitude variations across horizontal time slices reflect broad

lithologic variations within these marine deposits. Minor crenulationsalong these generally horizontal reflections are aligned through many

successive horizons and probably record deformation around gas pipes

through unconsolidated sediments. Small, high-sinuosity channels that

are imaged at about 400 ms twtt, and that are joined by larger, straighterchannels in horizons stratigraphically a bit higher, may reflect prograda-

tion of a distributive (delta top) fluvial system. Diffuse amplitude

variations observed in time slices in areas between these channel bodiesare broadly lobate, and may record lithologic variations across adjacent

mouth-bar or interdistributary-bay deposits.

The wide variety of channel sizes in the overlying sequences suggests

the presence of rivers that carried very different discharge. The largest

channels (kilometers wide and 25–50 m thick) are inferred to be depositsof major trunk rivers, whereas smaller channels of variable size and

planview geometry are inferred to be tributaries or floodplain drainage

channels. Reflection geometries that define bar accretion deposits and

channel fills within the largest channels (e.g., Fig. 7) suggest that they hada channel-forming cross-sectional area of about 60,000 m2. Although

accurate estimates of channel-forming discharge require information on

vertical trends in grain size within these channel deposits (which is not

available), broadly constrained estimates based on assuming a mean grain

size of fine sand suggest mean flow rates of about 0.6 m/s and thus







a channel-forming discharge of about 35,000 to 40,000 m3/s (see methods

in Willis 1993a). This suggests that the largest channel deposits imaged inthe study area were formed by rivers with discharge nearly as great asaverage floods of the modern Mekong River.

Vertical clusters of large channels along particular stratigraphicintervals, used to define the bases of sequences, are interpreted to recordperiods of lower accumulation rate relative to avulsion rate of the trunk

river(following standard sequence stratigraphicmodels for fluvial deposits;

Bridge and Leeder 1979; Shanley and McCabe 1993; Wright and Marriott1993). Intervals higher within sequences, with fewer and generally smallerchannel deposits, are interpreted to record periods of more rapidaggradation that led to increased preservation of tributary channels and

floodplain deposits. The standard interpretation of these types of verticalvariations is that channel incisions are related to sea-level falls, andsubsequent periods of floodplain aggradation are related to increasing

accommodation during sea-level rise. An alternative is that for fluvialsystems that decrease in slope onto a consistently low-gradient shelf, a fall

in sea level leads to fluvial floodplain aggradation as the river systemadjusts to greater distances to the regressing coastline (Summerfield 1985;Posamentier et al. 1992; Holbrook et al. 2006). Clusters of channels along

the base of sequences separating episodes of floodplain aggradation couldthen be interpreted to record more gradual erosion associated with bypass

of sediment basinward during continued sea-level fall and lowstand, ratherthan knickpoint erosion landward. In either case, interpretations of

a regional control on sequence development in this succession need to beviewed with some caution, because there likely were multiple river systemstraversing the study area and the region spanned by the seismic volume isprobably significantly smaller than the floodplain width across which the

main trunk river avulsed. Thus, it is possible that observed verticalvariations in fluvial architecture may also reflect longer-term lateral shifts

in thepositionof thetrunkriveror temporal changes in itsfloodplain widthrelated to adjustments of adjacent rivers and varying aggradation rate of their associated floodplains.

Tributaries cut into the floodplain adjacent to the larger trunk rivers, as

defined by distinctive dendritic gully systems observed in time slices, arethe best evidence for incision of the trunk river into the floodplain. These

features indicate the formation of valleys with adjacent interfluves

(Posamentier 2001). Such gullies are not expected to form adjacent tonon-incised river channels, because their growth to scales visible in

seismic slices is inhibited by overbank deposition during periodic riverfloods. In this study area gullies are observed to downcut only from

sequence boundaries.

In the study interval, there are increases in the abundance and extent of gullyformation along successive sequence boundaries. No evidence of gullyformation was observed cut into Sequence Boundary 1. Evidence of areally

restricted gullies is observed very locally along the most deeply incisedchannel along Sequence Boundary 2. Evidence of nearly continuous gully

formation, extending a few kilometers onto adjacent interfluves, isobserved along the most deeply incised channels of Sequence 3. The bestimaged and most extensive gullies extend broadly over many kilometers

across the amalgamated interfluves of Sequence Boundaries 4 and 5. More

extensive gully systems are interpreted to record longer periods of trunk-

river incision during the formation of successive sequence boundaries, and

perhaps also greater river incision depth.

Progressive decrease in mean sequence thickness and increase in gullyformation along successive sequence boundaries suggests that the upper

interval of the Muda Formation comprises a forward-stepping sequenceset. That is, the formation of successive sequence boundaries is inferred tobe associated with longer-term bypass of sediment, longer-term loss of accommodation, and possible regression of shorelines farther basinward.

The poorly imaged channels in the uppermost part of this sequence set(upper interval of Sequence 5; Fig. 4H) may indicate that channel-fill

lithologies became more similar to adjacent floodplain deposits duringinitial transgression. Deposits that cap Sequence 5 are thin (comprising at

most the upper 40–60 ms twtt of sediment), and probably formed duringcontinued marine transgression of this prograding sequence set. Thespecific horizon that records marine transgression is poorly imaged due to

the strength of the sea-floor reflection.

There are systematic changes in channel size and pattern upward withineach sequence (Fig. 7). The size of channels generally decreases upwardwithin each sequence. Although the deepest channels cut into sequence

boundaries clearly record incision greater than associated channel flowdepths (values greater than about 40 m), the thickness of bar accretion

deposits along inner banks of large channel bends suggest that 20–40 m

deep channels were common. Maximum relief along sequence boundariesis thus only slightly greater than the thickness of accretion sets associatedwith the largest individual channels, indicating that total depths of valleyincision were not much greater than the depths of the associated river

channels. Decrease in mean channel size upward within sequences reflectsdifferent dimensions of incised and overlying unincised major channels

and also preservation of smaller tributary and floodplain channels.

Sequence boundaries with better defined incision (i.e., Sequence

Boundaries 3–5) are overlain by higher sinuosity channels with moreobvious bar accretion deposits, and channels that incise from horizons

stratigraphically higher in these sequences are generally straighter. Thisobservation is contrary to the general assumption that steeper stream

gradients along the axis of an incised valley lead to straighter braidedchannel patterns, and that channels become more sinuous as slopesdecline during transgressive valley filling (Wright and Marriott 1993).

Near the center of the broad exposed Sunda shelf stream gradients mayhave been uniformly very low during Muda deposition. Thus, moresinuous major channels may record slopes steepened by incision and the

straighter, lower-sinuosity channels that show no evidence of lateralmigration may have flowed across lower gradients (Fig. 8). Upward

change in the sinuosity of larger channels from the base of Sequence 1 tothose that incise downward from the middle of this sequence may indicatethat the deepest channel in this non-incised sequence did not flow down

the steepest gradients. Given that the sinuous channels at the bases of themost deeply incised sequences are also the largest (as indicated by the

scale of inner-bank accretion deposits), it may alternatively be thatchannels with greater discharge had greater stream power relative tosediment load. In this case, their sinuous planform (relative to the ‘‘large’’channels higher in the same sequence) may reflect an increased ability of

these channels to erode their banks during high discharge, rather than

r

FIG. 5.—Map-view traces of channels compiled by combining observations from several successive time slices through the upper Muda Formation at Belida Field.Although mapped intervals of channels correspond in a general way to seismic slices shown in correspondingly labeled parts of Figure 4, the seismic slices are complicatedby channels that incise downward from intervals higher in the stratigraphy. A) Channels that incise downward from the interval below Sequence Boundary 1, between 412to 368 ms twtt. B) Channels that incise downward from the basal and middle intervals of Sequence 1, between 354 and 310 ms twtt. C) Channels that incise downwardfrom the upper interval of Sequence 1, between 306 and 278 ms twtt. D) Channels that incise downward from the basal interval of Sequence 2, between 278 and 250 mstwtt. E) Channels that incise downward from the upper interval of Sequence 2 and the most deeply incised deposits of Sequence 3, between 214 and 190 ms twtt. F)Channels that incise downward from the upper interval of Sequence 3 and most deeply incised deposits of Sequence 4, between 180 and 160 ms twtt. G) Channels thatincise downward from the uppermost interval of sequence 3, in sequence 4, and the lowermost interval of Sequence 5. H) Channels that incise downward from theuppermost intervals of Sequence 4 , between 134–114 ms twtt.




reflecting temporal changes in downstream gradients. The sinuosity of

smaller channels probably reflects more local stream gradients and

sediment loads, which could have been influenced by local floodplain

depositional features (e.g., levees and crevasse splays adjacent to the

larger channels). Thus, smaller channels are less likely to reflect regional

stratigraphic trends. For example, some small sinuous rivers alongSequence Boundary 5 appear to change downstream into straighter

incised gullies (Fig. 4G).

Origin of Sequences

The origin of sequences in the upper interval of the Muda Formation is

difficult to constrain from the limited area of this study. Posamentier

(2001) suggested fluvial incision can occur due to: (1) sea-level fall across

a region with steepening downstream gradients, for example across an

exposed shoreface or the continental shelf edge; (2) erosion of channels

across areas of tectonic uplift; and (3) climatic variations in river

discharge that leave underfit river deposits along the courses of larger-discharge channels. Although none of these mechanisms can be ruled out

definitively based on the data available from Belida field, they can be

assessed based on observed variations within sequences and the broader

depositional setting.

The Muda Formation at Belida field is located in middle parts of regional drainage systems that extended across much of the Sunda shelf during Pliocene to Holocene sea-level lowstands (Fig. 1; Murray 2003;

Murray and Dorobek 2004). Regional seismic profiles extending eastwardacross all of the West Natuna Basin and parts of the adjacent East

Natuna and Nam Con Son basins show that the Muda Formation (and

its lateral stratigraphic equivalents) vary little in thickness across the

nearly 1000 km distance to the present-day Sunda shelf edge (Dorobek,

unpublished). Sediment aggradation across the Sunda shelf thus appearsto have been broadly laterally consistent during Pliocene to Recent time.

This observation, and the repetitive nature of fluvial variations that

define sequences in the upper Muda Formation, argues against local

tectonic controls on fluvial aggradation and erosion rates.

Posamentier (2001) suggested that rivers crossing a low-gradient,

lowstand-exposed shelf are likely to remain non-incised over large areaswhen sea-level fall is not extensive enough to expose the shelf edge. To the

extent that this is true, a sea-level control on upper Muda Formationsequences would require that large regions of the Sunda shelf, perhaps

distances of 1000 km or more, responded essentially synchronously to

sea-level changes. Variations in the incision of interfluves observed on

successive sequence boundaries would then also suggest that gully

formation occurs very slowly relative to rates that trunk rivers incise

shelf-edge knickpoints landward across the shelf. Similarly, fluvialaggradation rates and channel behavior also would be required to

respond very rapidly across broad regions to downstream-gradient

declines as the shelf was episodically flooded. There is little evidence for

such extensive and rapid response of fluvial systems to high-frequency

sea-level variations, in as much as stream gradient changes required toadjust river profiles at distances of many hundreds of kilometers from the

shelf edge would be negligible. Burns et al. (1997) suggest that effects of

sea-level changes on river gradients should be only a few ‘‘backwater

lengths’’ (river depth divided by downstream slope), a distance that

should not exceed a few hundred kilometers, even considering the

probable low gradients of the exposed Sunda shelf.

r

FIG. 6.—Topographic maps of sequence boundaries defined by tracing specificreflections through the seismic volume of the upper Muda Formation atBelida Field.




An alternative mechanism for sea-level control on sequence formation

in the upper Muda Formation is that fluvial incision across a succession

of falling-stage shorelines on the shelf formed during episodic short-term

regressions and transgressions. This is supported by the modest depths of incision along sequence boundaries relative to sizes of the largest internal

channel deposits (less than two to one). Given expected low shelf

gradients, this model would still require significant regressions and

transgressions to allow the accumulation of shoreline deposits that are

thick enough to produce adequate fluvial incision, followed by very rapid

landward expansion of incised valleys cut into falling-stage shorelines

located basinward. Support for this idea would require identification of

coeval Muda Formation shoreline deposits basinward of Belida field.

Given evidence that this sequence set is dominantly regressive, it might be

expected from this model that younger sequences would be less deeply

incised as successive delta-front knickpoints shifted farther basinward

onto the shallow shelf. This supposition is not supported by observations

from this example.

Although climate controls on river discharge are difficult to constrain

from our available data, they would be expected given the icehouse

conditions of the Pliocene to Recent and low-latitude setting of the study

area. Climatically modulated changes in river discharge could affect river

channel size, sediment transport capacity, and patterns of erosion and

deposition over large areas of these drainage basins. Large changes in

river discharge during the Holocene caused by changes in monsoonal

precipitation patterns have been reported to occur in rivers that drain intothe Himalayan foredeep, as recorded by incision of floodplains extendingacross alluvial fans of the Ganges plains to low-lying areas on the top of

the Ganges–Brahmaputra delta (Goodbred 2003; Gibling et al. 2005).Whereas incision and changes in river pattern are expected to attenuate

landward away from shelf-edge knickpoints exposed during sea-levelfalls, effects of variations in river channel discharge caused by climatic

changes are more likely to influence the entire drainage basin. Bogart andvan Balen (2000) speculated that river incision may reflect lags betweenincreases in river water discharge and associated increases in sedimentsupply. The observation of more sinuous channels with better developed

bank accretion deposits along the most deeply incised areas of sequenceboundaries may support this supposition, in as much as it suggests that

incised rivers would have more stream power to erode their banks.Similarly, decrease in the size of the largest channels upward withinsequences may indicate declining river discharge relative to sediment

loads, rather than a backfilling of incised drainages due to declininggradients caused by sea-level rise.

DISCUSSION

Although sequence stratigraphic concepts have been widely applied tofluvial successions, most well constrained examples are from deposits

formed near the coast, where fluvial deposition can be related fairly

FIG. 7.—Close-up view of largest channel incised into Sequence Boundary 4, in horizontal time slice and cross section.

FIG. 8.—Dimensions and sinuosity of chan-nel-form reflections shown relative to the strati-graphic horizon from which they originated. Thesea-level curve of Haq et al. (1987) is shown onthe right.




directly to stacking patterns in shallow marine deposits and shoreline

regression–transgression trends. For example, where fluvial channels are

incised into regressive shoreface deposits, fluvial incisions are partially

filled with transgressive estuarine facies and the succession is capped by

a marine flooding surface (summaries in Shanley and McCabe 1993;

Zaitlin et al. 1994; Blum and Tornqvist 2000). For these examples

knickpoint erosion into a delta front edge exposed during sea level fall isassumed to have a major influence on valley development.

For successions deposited farther inland, sequence divisions are

generally defined based on vertical variations in the proportion of

channel to overbank deposits, and less commonly by recognizing laterally

continuous erosion surfaces, abrupt changes in sandstone petrography, or

intervals with mature paleosols (e.g., Aitken and Flint 1995; Legarreta

and Uliana 1988; Miall and Arush 2001; McCarthy and Plint 1998).

These interpretations tend to be more conjectural, however, because the

influence of sea level fluctuations are expected to attenuate landward and

thus, other allostratigraphic mechanisms that can control variations in

alluvial architecture become increasingly probable explanations for

observed variations. Increasing channel sandstone proportion is not

always associated with declining aggradation rate as predicted by sea-

level-driven alluvial sequence stratigraphic models (e.g., Read and Dean1985; Willis 1993b; and discussion of hypothetical cases in Heller and

Paola 1996), and several authors have suggested that in many cases fluvial

channels aggrade or simply extend basinward following sea level falls

rather than incising (Miall 1991; Posamentier 2001).

Given the prevalence of erosion surfaces of varying depth within fluvial

deposits, evidence for valley incision from outcrop exposures is generally

based on recognizing extensive erosion surfaces with relief significantly

greater than the thickness of individual channel bar accretion sets and

adjacent channel fills. In this paper we follow Posamentier (2001) in

suggesting that distinctive dendritic gullies adjacent to channel margins

observed in horizontal time slices of 3D seismic volumes are adequate

evidence to demonstrate that a river channel was incised into its

floodplain, despite basal erosion surfaces with nearly the same relief as

the thickness of adjacent point-bar deposits. The occurrence of similar

lowstand bypass channels of the Burdekin River across the low-gradient

shelf of northeastern Australia led Fielding et al. (2003, 2005) to propose

a distinction between ‘‘entrenched’’ channels and ‘‘incised’’ valley

deposits. Although entrenched channels have not been recognized in

outcrop, this may reflect a lack of observation rather than the absence of

these features. For example, in the Siwaliks of Pakistan the second author

of this paper observed multi-storied sandstone bodies that terminated at

cutbank margins against overbank successions that lacked levee deposits,

but he failed to walk out the surface correlative with the terminating basal

erosion surface of the channel sandstone body into the adjacent overbank

deposits to look carefully for evidence of gully formation.

Posamentier (2001) distinguished non-incised and incised lowstandchannels using seismic cross sections similar to those presented here, and

suggested that, although both types of channel bodies were depositedduring an overall fall in sea level, incised channels likely form only when

the sea level falls below the antecedent shelf edge. The channels hediscussed, in the southern Java Sea, were interpreted to record fluvialchannels and valleys cut directly into shelf deposits (i.e., regressions were

so rapid that prograding shallow marine deposits were not preserved).

The deposits imaged in this study are somewhat different, in as much asseveral hundred meters of net aggradation occurred during deposition of these sequences, basal deposits of this succession appear to be deltaic, and

the overall succession is interpreted to be progradational. Channels in thissystem episodically aggraded and then incised. The occurrence of deposits

formed by very large rivers suggests that regional drainages were free toavulse over wide areas of the Sunda shelf between episodic incisions,because it is unlikely that deposits of this large river are restricted by

chance to the small area covered by this study. In this setting, distinctionbetween non-incised, entrenched, and incised valley channel bodies ismore tenuous, and depends critically on the resolution in the seismicimage of features like bar accretion surfaces and interfluve gullies. There

may be a complete gradation between these types.

Where lowstand incision is not pronounced, as in this case, it becomes

difficult to distinguish channel incisions caused by climatically controlleddischarge variations, very subtle floodplain deformation, and landwardknickpoint erosion following sea-level falls. Channel incisions initiated bythese different mechanisms are unlikely to be regionally synchronous.Given that gully incisions appear to extend only short lateral distances

away from the entrenched channels (order of kilometers to a few tens of kilometers), it is not clear that the sequences defined here are of regional

extent. Episodic entrenchment and river avulsion during interveningperiods of floodplain aggradation may leave a series of laterallydiscontinuous falling-stage erosion surfaces rather than a single regional

allostratigraphic sequence boundary. Similarly, incisions into the shelf edge caused by knickpoint erosion following a sea-level fall may beregionally discontinuous, where river courses in areas upstream remainnon-incised and continue to avulse over time (Leeder and Stewart 1996;

Tornqvist et al. 2003).

Alluvial architecture models used to calculate subsurface channelsandstone connectivity generally assume a stationary distribution of channel bodies, on the basis of the underlying idea that floodplain

aggradation is dominated by levee growth adjacent to major channels,which expand at uniform rates to trigger a statistically constantdistribution of river channel avulsions through time (Leeder 1978; Allen

1978; Bridge and Leeder 1979). In this subsurface example, the largestchannels are incised and aggradational intervals appear to be dominated

by fluvial systems with smaller channels. Although the scale of the studyarea and seismic resolution of floodplain depositional elements may notbe adequate to define alluvial ridges adjacent to the major channels, anabundance of smaller channel systems within intervals that separate

major channel bodies agrees with models that predict floodplainaggradation dominantly occurs during avulsion events (Smith et al.1989) rather than the growth of extensive alluvial ridges. Miall (2006) also

noted that the wide variety of channel sizes and fluvial styles imaged in3D seismic data of the Pleistocene Pilong Formation (offshore Malaysia)

suggests pronounced changes in channel-body dimensions and perhapsdeposits of multiple river systems. This degree of complexity is notcurrently addressed in alluvial architecture models. High-frequency

episodes of channel entrenchment and aggradation, as observed in thisstudy, are also likely to increase horizontal relative to vertical channeldeposit connectively, compared to predictions for systems with equalchannel sandstone proportion formed under more uniformly aggrading

conditions and a stationary distribution of channel avulsions. Alluvialarchitecture models that can incorporate sequence stratigraphic trends

FIG. 9.— Relationship between slope and channel sinuosity defined by flumeexperiments of Schumm and Khan (1972).




also require better understanding of extrabasinal influences on patterns of fluvial deposition. In summary, the next generation of alluvial sequencestratigraphic models will likely require detailed 3D seismic images of a broader range of fluvial depositional systems as well as well-constraineddata on contemporaneous eustatic fluctuations and regional differentialsubsidence patterns.

CONCLUSIONS

The upper Muda Formation at Belida Field in the West Natuna Basinis a 225-meter-thick, progradational sequence set that coarsens upward

from marine shelf and deltaic deposits to fluvial deposits. These depositsare capped by modern marine deposits of the Sunda shelf. Five fluvialsequences, each of which is tens of meters thick, are defined by theclustering of channels along specific horizons that are separated byintervals with fewer channel deposits. Sequence boundaries are generallymarked by erosion greater than the thickness of bar accretion depositsadjacent to individual channels; gully formation on interfluves alsocharacterizes sequence boundaries. Deeper erosion and greater extent of gully formation on successive sequence boundaries suggests greater long-term loss in accommodation and greater bypass of sediment throughtime. Major channels in basal parts of the better developed sequences(Sequences 3 through 5) are larger and more sinuous, and show greater

preservation of bar accretion deposits than channels higher in thesesequences. These vertical changes may indicate that sequence-boundaryincision was associated with climatic changes in river discharge, ratherthan changes in river gradient associated with sea-level fluctuations. Thearchitecture of fluvial deltaic sequences deposited on a low-gradientcontinental shelf differs from better documented highstand examplesbecause sea-level fall can lead to fluvial aggradation and fluvial channelsmay not become deeply incised. Current sequence stratigraphic modelsfor fluvial deposits fail to address the variety of possible controls onalluvial architecture and the range of possible responses of fluvial systemsto changing allocyclic controls.

ACKNOWLEDGMENTS

This research was supported by a scholarship to the first author from theEducational Consortium of the Coordinating Board of Oil and Gas of Indonesia. Chuck Caughey of ConocoPhillips was especially supportive. Wealso thank the Belida Group of ConocoPhillips Indonesia in Jakarta,including Rahadian Adhyaksawan, Sugiharto Danudjaja, Paulus Hamid,Fadia Hamid, and Redo Waworuntu for help in acquisition of these data.Roald Brotherton and Vaughn Ball are thanked for permission to publish.

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Received 11 December 2005; accepted 30 September 2006.


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