An Online Guide to Sequence Stratigraphy：在线指南层序地层学.doc

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1、An Online Guide to Sequence StratigraphyThis online guide is primarily aimed at the application of sequence stratigraphy to outcrops. As a result, none of the examples deal with topics related specifically to cores, well logs, or most significantly, seismic. Perhaps the best way to work through this

2、 online guide is to start with accommodation and to continue down the list of topics from there. Many of the illustrations in this online introduction to sequence stratigraphy are modified from the figures in Van Wagoner et al.s Siliciclastic Sequence Stratigraphy in Well Logs, Cores, and Outcrops (

3、AAPG Methods in Exploration #7). Interested readers should study that reference and other references in the Further Reading section for a fuller explanation of the concepts introduced here. AccommodationThe Accommodation Space EquationOver long time scales (105 - 108 years), sediment accumulation is

4、 strongly controlled by changes in eustatic sea level, tectonic subsidence rates, and climatic effects on the production of sedimentary grains. Several of these factors are linked to one another through the accommodation space equation. This balance of terms is most easily explained for marine sedim

5、ents, but can be easily modified to include terrestrial sedimentation. A number of processes can cause the surface of the oceans to move up and down relative to the center of the earth. The distance from the sea surface to the center of the earth is eustatic sea level. In addition, the lithosphere c

6、an also move up and down relative to the center of the earth, and changes in the distance from some arbitrarily chosen reference horizon and the center of the earth are called uplift or subsidence. The distance between this reference horizon and the sea surface is called relative sea level or accomm

7、odation space. Acommmodation space can be filled with sediments or water. The distance between the sediment/water interface and the sea surface is known as water depth. The accommodation space not filled with water is filled with sediment. The rates of change of tectonic subsidence, eustatic sea lev

8、el, sediment thickness and water depth are linked to one another through the accommodation space equation: T + E = S + W where T is the rate of tectonic subsidence, E is the rate of eustatic sea-level rise, S is the rate of sedimentation, and W is the rate of water depth increase (or deepening). The

9、se four variables are defined such that positive values correspond to tectonic subsidence and eustatic sea-level rise (factors that increase accommodation space) and sediment accumulation and water depth increase (factors that reflect filling of accommodation space). Reversing the signs of these var

10、iables accommodates tectonic uplift, eustatic sea-level fall, erosion, and shallowing of water depth, respectively. The accommodation space equation represents a simple volume balance, with the terms on the left controlling the amount of space that can be occupied by sediments and water and the term

11、s on the right describing how much water or sediment fills the accommodation space. As written, the equation is an approximation. In reality, sediment thickness and water depth must be corrected for compaction of sediments and for the isostatic effects of newly deposited sediment. Through section me

12、asurement, changes in sediment thickness can be known, and through facies analysis, changes in water depth can be known or approximated. However, without outside information, the rates of eustatic sea-level change and tectonic subsidence cannot be isolated, nor can their effects be distinguished fro

13、m one another for a single outcrop. In other words, there is no unique solution to this equation as it has two unknowns. Thus, it is impossible in most cases to ascribe water depth or sedimentation changes to eustasy or tectonics without having regional control or outside information. Backstripping

14、is a method of analysis that iteratively solves the accommodation space to measure changes in relative sealevel through time. Although as pointed out earlier that no unique solution exists for this equation, solving it for relative sea level can provide useful insights into eustasy and tectonics. Th

15、ese data may then be used to date the timing of rifting and orogeny, to constrain estimates of lithospheric thickness, and to understand global CO2 cycles and global patterns of sedimentation. Causes of Eustatic Sea-Level ChangeChanges in eustatic sea level arise from either changes in the volume of

16、 ocean basins or changes in the volume of water within those basins. The volume of ocean basins is controlled primarily by the rate of seafloor spreading and secondarily by sedimentation in ocean basins. Because hot and young oceanic lithosphere is relatively buoyant, it floats higher on the astheno

17、sphere and displaces oceanic waters upwards and onto continents. Older and colder oceanic lithosphere is denser, floats lower on the asthenosphere, and allows oceanic waters to stay within ocean basins. Long-term (102 k.y. - 105 k.y.) changes in the global rate of seafloor spreading can change the g

18、lobal average age and density of oceanic lithosphere, resulting in tens to a couple hundred meters of eustatic change. Filling of ocean basins with sediments derived from continental weathering is a relatively slow and minor way of changing ocean basin volumes and is capable of meters to tens of met

19、ers of eustatic change over tens to hundreds of millions of years. The three most important controls on the volume of seawater are glaciation, ocean temperature, and the volume of groundwater. Continental and mountain glaciation is perhaps the most efficient and rapid means of storing and releasing

20、ocean water. Due to Archimedes principle, ice caps over polar oceans do not affect eustatic sea level, so frozen seawater must be placed on a landmass to lower eustatic sea-level. Continental glaciation is capable of driving high amplitude (10 - 100 m) and high frequency (1 - 100 k.y.) eustatic chan

21、ges. Because water expands at temperatures higher and lower than 4 degrees C, and because the depths of the oceans average around 5 km, small changes in the temperature of seawater can lead to significant changes in ocean water volume. Changes in water temperature can drive a few meters of eustatic

22、change over short time scales (0.1 - 10 k.y.). Ocean water is continuously being recycled through continents as groundwater and surface water, such as rivers and lakes. Over relatively short time scales (0.1 - 100 k.y.), changes in the amount of water sequestered on the continents can cause up to a

23、few meters of eustatic change. Causes of Tectonic SubsidenceTectonic subsidence is also called driving subsidence and is distinguished from the isostatic effects of sediment and water loads. Tectonic subsidence, as its name implies, is driven by tectonic forces that affect how continental lithospher

24、e floats on the asthenosphere. Three main mechanisms that affect this isostatic balance and therefore drive tectonic subsidence include stretching, cooling, and loading. Stretching of continental lithosphere in most situations results in the replacement of relatively light continental lithosphere wi

25、th denser asthenosphere. The resulting stretched and thinned lithosphere sinks, causing tectonic subsidence. Stretching occurs in several types of sedimentary basins including rifts, aulacogens, backarc basins, and cratonic basins. Cooling commonly goes hand-in-hand with stretching. During stretchin

26、g, continental lithosphere is heated, becomes less dense, and tends to uplift from its decreased density (the net effect in a stretched and heated basin may result either in uplift or in subsidence). As continental lithosphere cools, it becomes denser and subsides. Cooling subsidence decreases expon

27、entially with time yet can cause a significant amount of subsidence hundreds of millions of years following initial cooling. Cooling subsidence is especially important on passive margins and in cratonic basins. Tectonic loading can also produce subsidence. The additional weight of tectonic loads suc

28、h as accretionary wedges or fold and thrust belts causes continental lithosphere to sink, leading to tectonic subsidence. Because the lithosphere responds flexurally, the subsidence occurs not only immediately underneath the load, but in broad region surrounding the load. Tectonic loading is particu

29、larly important in orogenic regions such as foreland basins. ParasequencesExpressionParasequences are defined as a relatively conformable succession of genetically related beds or bedsets bounded by marine flooding surfaces and their correlative surfaces. In addition to these defining characteristic

30、s, most parasequences are asymmetical shallowing-upward sedimentary cycles. By genetically related, it is meant that all facies within a parasequence were deposited in lateral continuity to one another, that is, Walthers Law holds true within a parasequence. So, for a typical siliciclastic wave-domi

31、nated shoreline, a particular suite of facies should occur in a predictable order. A parasequence that spanned all of these facies would begin with bioturbated offshore mudstones, pass through the storm beds of the transition zone or lower shoreface, continue through the trough crossbedding of the s

32、horeface, pass upwards into the seaward inclined laminae of the foreshore, and be capped by a backshore or coastal plain coal bed. In reality, a single parasequence at a single outcrop rarely passes through all of these facies, but instead includes only a portion of this facies succession; however,

33、all of the facies that do occur appear in the correct order as predicted by Walthers Law. For example, a typical sandy wave-dominated parasequence in an outcrop might include only offshore and transition zone facies, or only shoreface, foreshore, and coastal plain facies, but offshore facies would n

34、ot be overlain by coastal plain facies within a single parasequence. A parasequence along a deltaic coastline would show a similar coarsening-upward succession, although it would differ in the sedimentary structures developed. A parasequence developed on a muddy siliciclastic shoreline would have a

35、different suite of facies, but they would also be arrayed vertically in a shallowing upward order and facies relationships would obey Walthers Law. A typical muddy shoreline parasequence would start with cross-bedded subtidal sands, continue with interbedded bioturbated mudstones and rippled sands o

36、f the intertidal, and pass upwards into entirely bioturbated and possibly coaly mudstones of the supratidal. The flooding surfaces that define the top and base of a parasequence display abrupt contacts of relatively deeper-water facies lying directly on top of relatively shallow-water facies. Rocks

37、lying above and below a flooding surface commonly represent non-adjacent facies, such as offshore shales directly overlying foreshore sands or basinal shales directly overlying mid-fan turbidites. Thus, Walthers Law cannot be applied across flooding surfaces. Given that many parasequences are meters

38、 to tens of meters thick, this radically reduces the scale at which Walthers Law can be applied. Cases where Walthers Law has been applied to sections hundreds to thousands of meters thick are nearly always incorrect. Flooding surfaces may also exhibit small scale erosion, usually of a meter or less

39、. Flooding surfaces may be mantled by a transgressive lag composed of shells, shale intraclasts, calcareous nodules, or siliciclastic gravel; such lags are usually thin, less than a meter thick. Flooding surfaces may display evidence of firmgrounds, such as Glossifungites ichnofacies, or hardgrounds

40、 that may be bored, encrusted, and possibly mineralized. Origin and ScaleA parasequence represents a single episode of progradation, that is, the seaward movement of a shoreline. This seaward shoreline movement produces the familiar shallowing-upward succession seen within parasequences. The shallow

41、ing-upward succession indicates that accommodation space is being filled more rapidly than it is being created, and some evidence suggests that in some cases, accommodation space is created only at flooding surfaces and not during the bulk of a parasequence. Flooding surfaces represent a relative ri

42、se in sea level, such that accommodation space is being created at a faster rate than it is being filled with sediment. Although these rapid rises in accommodation space are commonly attributed to eustatic sea-level rise, some flooding surfaces are clearly attributable to earthquake-induced subsiden

43、ce or to delta switching or similar autocyclic mechanisms. Scale is not part of the definition of a parasequence. However, parasequences are commonly meters to tens of meters thick and they commonly represent durations of tens to hundreds of thousands of years. Many authors confuse these typical sca

44、les with the definition of a parasequence, and erroneously assume that any small cycle must be a parasequence and that any long or thick cycle cannot be a parasequence. This is not the case as some meter-thick cycles clearly do not have a parasequence structure and some hundred to thousand meter-thi

45、ck cycles do display a parasequence structure. Lateral and Vertical Relationships within a ParasequenceOne of the most powerful aspects to recognizing parasequences is understanding and applying the predictable vertical and lateral facies relationships within parasequences. As stated earlier, facies

46、 reflect increasingly shallower environments upwards within a parasequence. Although a complete vertical succession of facies can be compiled from a suite of parasequences, most parasequences will display only a portion of the entire shallowing-upward succession of facies. figure adapted from Van Wa

47、goner et al. (1990)Because shallow water facies within a parasequence will pinch out laterally in a downdip direction and deeper water facies within a parasequence will pinch out in an updip direction, the facies composition of a single parasequence changes predictably updip and downdip. Thus, a sin

48、gle parasequence will not be composed of the same facies everywhere, but will be composed of deeper water facies downdip and shallower water facies updip, as would be expected. Because parasequence boundaries represent a primary depositional surface, that is, topography at the time of deposition, fl

49、ooding surfaces will tend to be relatively flat but dip slightly seaward at angles typical of continental shelves. Finally, parasequence boundaries may become obscure in coastal plain settings and in deep marine settings because of a lack of facies contrast necessary to make flooding surfaces visible. Parasequence Sets and Stacking PatternsIn most cases, there will not be simply one parasequence by itself, but there will be a series of parasequences. Sets of successive parasequences may disp