Differences between carbonates and siliciclastics
Siliciclastic and carbonate sedimentary bodies are subdivided
by similar surfaces that are responses to changes in base level. Differences in the sequence stratigraphy of these sediment
types are related to carbonate accumulation tending to be "in situ
production" while siliciclastics are transported to their depositional setting.
Rates of carbonate production are greatest close to the air/sea interface since they are linked to photosynthesis and so depth-dependent. Thus carbonate facies and their fabrics are clear indicators of sea level position. Carbonate organisms can produce and accumulate
above certain hydrodynamic thresholds, an effect influenced by their biology
and the chemistry of the water known as ecological accommodation (Pomar (2001 a,
and b). Whereas siliciclastics, which only respond to hydrodynamic thresholds, are limited by their physical accommodation. Thus the character of carbonate sediment changes as organisms evolve, the plate tectonic
configuration of the depositional setting of the basin responds to pale-climate
change, and/or changes in paleogeography related to isolation or access to the
open sea. This means that carbonates can be used as indicators of depositional
setting that, when combined with sequence stratigraphy, make carbonate facies
analysis a powerful tool for the interpretation of the geological section and
prediction away from data rich areas.
It should be emphasized that, as has been shown by Fischer (1964), Pomar and Ward (1999), Goldhammer, et al, (1990), and D'Argenio et al (1997) that though shallow cycles of carbonate are composed of a relatively conformable succession of genetically related beds or bedsets these cycles are often truncated and incomplete so that maximum flooding and trangressive surfaces can be missing. This means that these cycles are not, in the strictest sense, a match for the clastic models of parasequences of Van Wagoner et al, (1999). Never the less we argue cycles can be used like parasequences in the analysis of the sedimentary section as units of process/product oriented depositional models. However should they exhibit truncated cycles and miss the sediments of an initial transgression or maximum flooding event one should consider them as high frequency carbonate cycles, not parasequences.
Response of carbonates to relative sea level change - Links to movies, exercises & .pdf files.
Lower rates of carbonate accumulation
of interior shelf produce lagoon which gives up in response to sea level rise.
Early Cretaceous Shaybah formation
, UAE, carbonate
margin responds to sea level change (Kendall et al, 2000) (below
s of Miocene of Mallorca capture sea level history (Pomar, 1991). Outcrop Exercise
Upper Devonian Judy Creek carbonate
build up responds and "Gives up" with sea level change (Scaturo, et al, 1989),
Sedpak simulation of evolving carbonate
and clastic geometries and cross section responding to changing base level
. Link to full explanation
The carbonate cycle of a sigmoid versus parasequence explained
The basic reefal accretional unit of the Miocene reef complex of Mallorca is the "sigmoid
". This is bounded by clear erosion surfaces
(the product of sea level lowering and erosion with a matching correlative surface downdip) but has no obvious marine flooding surface
s . Updip and landward the sigmoid
is represented by a horizontal lagoonal bed
ward passes in sigmoid
al bedded reef-core lithofacies
belt and seaward into clinoform
bedded forereef slope beds
and sub-horizontal basinal lithofacies
. The bounda
ry over the lagoonal and reef-core lithofacies
of the sigmoid
is formed by an erosional surface that basinward becomes a correlative conformable surface in the reef slope and basin lithofacies
. Notably, the coral-morphology zonation within the reef-core facies of the sigmoid
migrates seaward, aggrades vertically, or moves landward over the bounding erosional surfaces
. This enables the sigmoid
(like system's tracts) to be tied to specific segments of the sea-level curve. Consequently the sigmoid configuration
can be considered "genetically" as a depositional sequence
, though not exactly fitting the original definition of a parasequence
. This is because the sigmoid
, like the parasequence
, is composed of a relatively conformable succession of genetically related beds
s . Also the geometric patterns shown by stacked sigmoid
s can be used, along with their position within a sequence
, like the patterns of stacked parasequence set
s, to define system-tracts , while within lower order depositional sequence
s there are sigmoid
cosets and megasets.
In the interests of keeping the sequence stratigraphic literature from becoming over complex it is argued here that during the time interval between the development of the erosional surface on the underlying sigmoid and the deposition of sediment marking the boundary of the overlying sigmoid, sea level dropped to be followed by a trangressive flooding event and the development of a maximum flooding surface. However since no sedimentary fill has been recognized that records these events, the sigmoid cannot be inferred to be equivalent to the parasequence, or vice versa! Similarly this "simplification" should not be applied to a shoaling upward carbonate cycle missing transgressive or maximum flooding sediments. In this case the transgression surfaces (TS) and maximum flooding surfaces (mfs) are not equivalent to erosion surfaces initially produced by a sea level fall, since the missing sediments mean that one cannot establish how the erosion surface was modified on the following transgression. Clearly the truncated high frequency carbonate cycle may have different genetic elements to a parasequence and should not be considered to be one! It should be noted that because "modern" type of reefal systems are able to build rigid frameworks, resistant to wave energy, this depositional system has the capacity to record even the highest-frequency sea-level cycles. Thus some sigmoids appear to record 7th order sea-level cycles that represent a periodicity of few-thousand years! Other depositional systems that have not produced this "rigid framework" to the sea level are not able to record such high-frequency cycles of sea level and parasequences may form.
Pomar (personal communication, 2004) proposes that parasequences form in response to sea-level para-cycles (rise and stillstand of sea level), commonly as a response of sea-level cyclicity when subsidence equals or exceeds the amount of sea-level fall, OR when the sedimentary systems are dominated by loose grains. In this latter case, lowering of base level (related to the fall in sea level) would increase basinward shedding of sediment and these erosional processes onto a granular seabed would not be recorded as an erosion surface. This could be the reason that higher-frequency sequences (simple sequences in Vail's definition) at the most commonly record up to 5th-order cycles of sea level. These high frequency carbonate cycles that have the genetic elements of the parasequence are "of course" carbonate parasequences.
Some carbonate parasequence geometries - Tools for the interpretation of depositional setting
The sequence stratigraphy of the carbonate sections is commonly determined from a combination of 2 and 3 D Seismic data (providing a comparatively low frequency resolution), well logs (providing a comparatively high frequency resolution), cores (providing very high frequency resolution) and outcrops (with best access to a combination of high frequency resolution and low frequency resolution).
|Click thumbnail to access the large images
The analysis of the sequence stratigraphy of carbonates is improved by applying the recent realizations of Larue et al (1995); Sprague et al, (2002); Sprague et al, (2003); and Sprague et al, (2004) for depositional systems and integrating:
Thus, as with clastic sediments (Sprague et al, 2002), at a general level the physical stratigraphy of the carbonate strata can be broken down into a hierarchical framework. This framework ties together genetically related architectural elements and their associated boundaries . The hierarchy of these elements is independent of the thickness and the time invovled in their accumulation. A top down breakdown of the architectural elements shows a progressive decrease in scale from the complex facies geometries of the basin margin to single tidal flat cycles or beds that accumulated on shallow shelves or in shallow lagoons. As Sprague et al, (2002) showed for clastics, these carbonate hierarchical elements are directly relatable to stratal units defined on the basis of sequence stratigraphy. Biostratigraphic data tied to the stratal units enable the direct comparison between shallow-marine and deeper marine carbonate sequences and their related units with the potential of correlation of the carbonate cycles to base level rise and fall.
All are the combined products of base level change. This is particularly true of shallow water carbonate accumulations which are depth dependent, a response to the paleo-oceanography, and processes of the depositional setting. The result of such an analysis creates a "powerful" framework of parasequence and high frequency cycle geometries that can be used to explain, assess and predict reservoir and aquifer quality better independent of thickness and time.
This approach even applies in deepwater settings. For instance, using the Tamabra formation of the Poza Rica Field Area of Mexico as an example, Loucks, et al (2006) have demonstrated that deeperwater mass-transport carbonate deposits are carried by gravity flow and suspension processes into deepwater basinal settings downslope from margins tied to shallow-water carbonate platforms. So while reefal and grain-rich debris accumulate on the shallow platform carbonate debris wedges extend into the deeperwater basin.
The architecture of this debris wedge is related to the availability of source material during changes in relative sea-level (Loucks, et al., 2006). During sea-level lowstands and transgressions or during early highstands when the platform rapidly aggrades, debris and mud flows composed of platform and slope carbonate mud, sand, and clasts generally accumulate. In contrast during highstands of sea level when the platform is flooded and shedding, density-flow and turbidite deposits composed of carbonate sand and lesser amounts of lime mud collect.
Click thumbnail to access the large images and click on the larger image to see them full size!
Geometries of carbonate strata
The geometries of carbonate strata are products of the shape of the depositional surface , changing base level and sediment accumulation. They are defined by the underlying and overlying surfaces. These surfaces may be the products of deposition and/or erosion and can coincide with the depositional event or proceed or follow this. Physical erosion, burrowing, boring, dissolution (Clari et al, 1995; Lukasik & James, 2003), and/or cementation may have modified them. Whatever their origin, these surfaces provide a convenient means to subdivide the carbonate section. From the perspective of sequence stratigraphy these surfaces are used to determine the order in which strata are laid down and define the geometries that they enclose.
As with the products of other sedimentary depositional systems carbonate strata exhibit a hierarchy of scales that include at the small-scale end ( beds , bed sets , and bed cosets) and at the larger spatial scales reef complexes, basin margin and slope complexes etc. These strata can be expressed as unconfined sheets, unconfined but localized build ups (reefs, banks and islands), unconfined but localized sigmoids (reef cores of Pomar 1991), bank margins etc., and confined incised channels (tidal channels and the products of flood events). What ever the final geometry this is the product of both accumulation (aggradation ) and erosion.
A set of carbonate sequence stratigraphy exercises
Click on the highlighted title above to access the exercises that are available on this site to examine the hierarchy of scales expressed by carbonate strata. These may be the lower frequency subdivisions that can be interpreted from seismic, or higher frequency subdivisions outcrop and well logs. These consider facies or more complex lithofacies assemblages from the perspective of sequence-stratigraphic concepts, including systems tracts, parasequences, sequences and their response to seal level rise ( TST), still stand (HST) fall (FSST) and lowstand (LST) and their response to the paleo-oceanography and processes of the depositional setting. The exercises are intended to develop skills that can be used to establish direct relationships between the nature of the carbonate bodies, the sequence stratigraphic architecture, reservoir connectivity, reservoir characterization and prediction. This would involve the use of systematic hierarchical relationships, integration of seismic, well, and core data with outcrop and subsurface analogs. From this you will gain a better understanding of how to predict accurate net-to-gross, continuity, architecture, and reservoir extent. If you are able to integrate biostratigraphy with your studies this will provide an independent time framework correlation made to cycles of base level rise and fall.
To conclude, carbonate depositional facies hierarchy provides a framework for the systematic description and comparison of carbonate deposits that is based on the physical relationships of strata and their boundaries. The recognition of genetically related stratigraphic elements, is independent of the lithofacies assemblage of carbonate, and is applicable at all scales.
Publications on the response of carbonates to sea level
Link to a page that lists some of the literature on the carbonate sedimentary record and how its sequence stratigraphic character varies in response to base level change, usually eustasy and gain access to .pdf files of these papers.
Bosence, D.W.J., Pomar, L., Waltham, D.A. Lankaster, T., 1994. Computer modeling a Miocene carbonate platform, Mallorca, Spain. Arnerican Association of Petroleurn Geologists Bulletin, 78:247-266.
Kendall, Christopher G. St. C., Abdulrahman. S. Alsharhan, Kurt Johnston and Sean R. Ryan; 2000; "Can The Sedimentary Record Be Dated From A Sea-Level Chart? Examples from the Aptian of the UAE and Alaska". In A. S. Alsharhan and R. W. Scott, Eds, Society of Economic Petrologists and Mineralogists (SEPM) Special Publication 69 on the Jurassic/Cretaceous Platform-basin Systems; Middle East Models; p 65-76 (Reference for the simulation of Shaybah Formation above )
Loucks, R. G., Charles Kerans, and Alfredo Marhx, 2006, "Origin and Organization of Mass-Transported carbonate Debris in the Lower Cretaceous (Albian) Tamabra formation, Poza Rica Field Area, Mexico", SEPM Research Symposium: The Significance of Mass Transport Deposits in Deepwater Environments II, AAPG Annual Convention, April 9-12, 2006 Technical Program
Pomar, L. and Ward, W.C. 1994. Response of a Miocene carbonate platform to high-frequency eustasy. Geology, 22:131-134.
Pomar, L. and Ward, W.C, 1995. Sea level change, carbonate production and platform architecture, in B. Haq ed., sequence stratigraphy and depositional response to eustatic, tectonic and climatic forcing, Kluwer Academic Press. p. 87-112.
Pomar, L., 2001 (a), Ecological control of sedimentary accommodation: evolution from a carbonate ramp to rimmed shelf, Upper Miocene, Balearic Islands: Palaeogeography, Palaeoclimatology, Palaeoecology, v. 175, p. 249-272.
Pomar, L., 2001 (b), Types of carbonate platforms, a genetic approach: basin Research, v. 13, p. 313-334.
References on a Hierarchical Approach to sequence stratigraphy
D. K. Larue, A. R. Sprague, P. E. Patterson , J. C. Van Wagoner (1995): Multi-Storey Sandstone Bodies, sequence stratigraphy, and Fluvial Reservoir Connectivity, Bulletin AAPG, (Abstract) AAPG Annual Meeting, 79, 13, 54
Sprague,A. R., P. E. Patterson, R.E. Hill, C.R. Jones, K. M. Campion, J.C. Van Wagoner, M. D. Sullivan, D.K. Larue, H.R. Feldman, T.M. Demko, R.W. Wellner, J.K. Geslin1 (2002), The Physical stratigraphy of Fluvial strata: A Hierarchical Approach to the Analysis of Genetically Related Stratigraphic Elements for Improved Reservoir Prediction, (Abstract) AAPG Annual Meeting
Sprague, A. R., M. D. Sullivan, K. M. Campion, G. N. Jensen, F. J. Goulding, T. R. Garfield, D. K. Sickafoose, C. Rossen, D. C. Jennette, R. T. Beaubouef, V. Abreu, J. Ardill, M. L. Porter, and F. B. Zelt, (2003), The Physical stratigraphy of Deep-Water strata: A Hierarchical Approach to the Analysis of Genetically Related Stratigraphic Elements for Improved Reservoir Prediction, AAPG Bulletin, (Abstract) AAPG Annual Meeting,.87, 10 p
Sprague, A. R., P.E. Patterson, M.D. Sullivan, K.M. Campion, C.R. Jones, T.R. Garfield, D.K. Sickafoose, D.C. Jennette, G.N. Jensen, R.T. Beaubouef, F.J. Goulding, J.C. Van Wagoner, R.W. Wellner, D.K. Larue, C. Rossen, R.E. Hill, J.K. Geslin, H.R. Feldman, T.M. Demko, V. Abreu, F.B. Zelt, J. Ardill, and M.L. Porter (2004), Physical stratigraphy of Clastic strata: A Hierarchical Approach to the Analysis of Genetically Related Stratigraphic Elements for Improved Reservoir Prediction, ABSTRACT, AAPG 2003-04 Distinguished lecturer Tour Information.