Difference between revisions of "Influence of depositional environment on sandstone diagenesis"
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| part = Predicting the occurrence of oil and gas traps | | part = Predicting the occurrence of oil and gas traps | ||
| chapter = Predicting reservoir system quality and performance | | chapter = Predicting reservoir system quality and performance | ||
| − | | frompg = 9- | + | | frompg = 9-83 |
| − | | topg = 9- | + | | topg = 9-85 |
| author = Dan J. Hartmann, Edward A. Beaumont | | author = Dan J. Hartmann, Edward A. Beaumont | ||
| link = http://archives.datapages.com/data/specpubs/beaumont/ch09/ch09.htm | | link = http://archives.datapages.com/data/specpubs/beaumont/ch09/ch09.htm | ||
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| − | Depositional environment influences many aspects of sandstone diagenesis. The flow chart | + | Depositional environment influences many aspects of sandstone [[diagenesis]]. The flow chart in [[:file:predicting-reservoir-system-quality-and-performance_fig9-51.png|Figure 1]] shows the interrelationship of depositional environment with the many factors controlling sandstone diagenesis. |
| − | [[file:predicting-reservoir-system-quality-and-performance_fig9-51.png|thumb|{{figure number| | + | [[file:predicting-reservoir-system-quality-and-performance_fig9-51.png|400px|thumb|{{figure number|1}}Flow chart showing the interrelationship of depositional environment with the many factors controlling sandstone diagenesis. After Stonecipher et al.<ref name=ch09r60>Stonecipher, S. A., R. D. Winn, Jr., and M. G. Bishop, 1984, [http://archives.datapages.com/data/specpubs/sandsto2/data/a059/a059/0001/0250/0289.htm Diagenesis of the Frontier Formation, Moxa Arch: a function of sandstone geometry, texture and composition, and fluid flux], in D. A. McDonald, and R. C. Surdam eds., Clastic Diagenesis: AAPG Memoir 37, p. 289–316.</ref>]] |
==Sediment texture and composition== | ==Sediment texture and composition== | ||
| − | Depositional environment affects sediment composition by determining the amount of reworking and sorting by size or hydraulic equivalence. Sediments that have a higher degree of reworking are more mechanically and chemically stable. The energy level of depositional environments affects sorting by size or hydraulic equivalence and consequently produces different detrital mineral suites | + | Depositional environment affects sediment composition by determining the amount of reworking and [[Core_description#Maturity|sorting]] by size or hydraulic equivalence. Sediments that have a higher degree of reworking are more mechanically and chemically stable. The energy level of depositional environments affects sorting by size or hydraulic equivalence and consequently produces different detrital mineral suites.<ref name=Stonecipher&May1990>Stonecipher, S. A., and J. A. May, 1990, [http://archives.datapages.com/data/specpubs/resmi1/data/a065/a065/0001/0000/0025.htm Facies controls on early diagenesis: Wilcox Group, Texas Gulf Coast], in D. Meshri and P. J. Ortoleva, eds., Prediction of Reservoir Quality Through Chemical Modeling, I: AAPG Memoir 49, p. 25–44.</ref> |
| − | For example, different facies of the Wilcox Group along the Gulf Coast of Texas have different compositions that are independent of their source area | + | For example, different facies of the Wilcox Group along the Gulf Coast of Texas have different compositions that are independent of their source area.<ref name=Stonecipher&May1990 /> Wilcox basal fluvial point bar sands are the coarsest and contain the highest proportion of nondisaggregated lithic fragments. Prodelta sands, deposited in a more distal setting, contain fine [[quartz]], micas, and detrital clays that are products of disaggregation. Reworked sands, such as shoreline or tidal sands, are more quartzose. |
==Depositional pore-water chemistry== | ==Depositional pore-water chemistry== | ||
| − | Depositional pore-water chemistry of a sandstone is a function of depositional environment. Marine sediments typically have alkaline pore water. Nonmarine sediments have pore water with a variety of chemistries. In nonmarine sediments deposited in conditions that were warm and wet, the pore water is initially either acidic or anoxic and has a high concentration of dissolved mineral species.<ref name=ch09r7>Burley, S. | + | Depositional pore-water chemistry of a sandstone is a function of depositional environment. Marine sediments typically have alkaline pore water. Nonmarine sediments have pore water with a variety of chemistries. In nonmarine sediments deposited in conditions that were warm and wet, the pore water is initially either acidic or anoxic and has a high concentration of dissolved mineral species.<ref name=ch09r7>Burley, S. D., J. D. Kantorowicz, and B. Waugh, 1985, Clastic diagenesis, in P. J. Brenchley, and B. P. J. Williams, eds., Sedimentology: Recent Developments and Applied Aspects: London, Blackwell Scientific Publications, p. 189–228.</ref> |
==Marine pore-water chemistry== | ==Marine pore-water chemistry== | ||
| Line 30: | Line 30: | ||
==Marine diagenesis== | ==Marine diagenesis== | ||
| − | |||
| − | + | [[file:predicting-reservoir-system-quality-and-performance_fig9-52.png|300px|thumb|{{figure number|2}} Typical diagenetic pathways for marine sediments. Copyright: Burley et al.;<ref name=ch09r7 /> courtesy Blackwell Scientific.]] | |
| − | [[file:predicting-reservoir-system-quality-and-performance_fig9-52.png| | + | The precipitation of cements in quartzarenites and subarkoses deposited in a marine environment tends to follow a predictable pattern beginning with clay authigenesis associated with [[quartz]] and feldspar overgrowths, followed by carbonate precipitation. Clay minerals form first because they precipitate more easily than quartz and feldspar overgrowths, which require more ordered crystal growth. Carbonate cement stops the further diagenesis of aluminosilicate minerals. |
| + | |||
| + | The diagram in [[:file:predicting-reservoir-system-quality-and-performance_fig9-52.png|Figure 2]] summarizes typical diagenetic pathways for marine sediments. | ||
==Nonmarine pore-water chemistry and cements== | ==Nonmarine pore-water chemistry and cements== | ||
| + | |||
| + | [[file:predicting-reservoir-system-quality-and-performance_fig9-53.png|300px|thumb|{{figure number|3}}Typical diagenetic pathways for warm and wet nonmarine sediments. Copyright: Burley et al.;<ref name=ch09r7 /> courtesy Blackwell Scientific.]] | ||
| + | |||
Nonmarine pore-water chemistry falls into two climatic categories: (1) warm and wet or (2) hot and dry. The chemistry of pore waters formed in warm and wet conditions is usually acidic or anoxic with large concentrations of dissolved mineral species. The interaction of organic material with pore water is a critical factor with these waters. The depositional pore water of sediments deposited in hot and dry conditions is typically slightly alkaline and dilute. | Nonmarine pore-water chemistry falls into two climatic categories: (1) warm and wet or (2) hot and dry. The chemistry of pore waters formed in warm and wet conditions is usually acidic or anoxic with large concentrations of dissolved mineral species. The interaction of organic material with pore water is a critical factor with these waters. The depositional pore water of sediments deposited in hot and dry conditions is typically slightly alkaline and dilute. | ||
| − | The diagram | + | The diagram in [[:file:predicting-reservoir-system-quality-and-performance_fig9-53.png|Figure 3]] shows typical diagenetic pathways for warm and wet nonmarine sediments. |
| − | |||
| − | [[file:predicting-reservoir-system-quality-and-performance_fig9-53.png| | ||
==Cements== | ==Cements== | ||
| − | The table below, compiled from data by Thomas | + | The table below, compiled from data by Thomas<ref>Thomas, R., 1983, An introduction to the thin section analysis of the diagenetic histories of clastic rocks, in I. Hutcheon, A. Oldershaw, and R. Thomas, eds., Clastic diagenesis: Canadian Society of Petroleum Geologists Short Course, University of Calgary, chapter 3, 56 p.</ref> shows the cements that generally characterize specific depositional environments. |
{| class = "wikitable" | {| class = "wikitable" | ||
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| rowspan="2" | Eolian | | rowspan="2" | Eolian | ||
| Dune | | Dune | ||
| − | | Quartz overgrowths dominate; also clay coats | + | | [[Quartz]] overgrowths dominate; also clay coats |
|- | |- | ||
| Interdune | | Interdune | ||
| − | | Grain-coating clays; in areas that were alternately moist and dry anhydrite, dolomite, or calcite common | + | | Grain-coating clays; in areas that were alternately moist and dry [[anhydrite]], [[dolomite]], or calcite common |
|- | |- | ||
| − | | Fluvial | + | | rowspan="2" | Fluvial |
| Flood plain | | Flood plain | ||
| Chlorite, illite, smectite, and mixed-layer clay | | Chlorite, illite, smectite, and mixed-layer clay | ||
| Line 80: | Line 82: | ||
==Diagenesis and depositional pore waters== | ==Diagenesis and depositional pore waters== | ||
| − | In the Wilcox of the Texas Gulf Coast, certain minerals precipitate as a result of the influence of depositional pore-water chemistry:<ref name= | + | In the Wilcox of the Texas Gulf Coast, certain minerals precipitate as a result of the influence of depositional pore-water chemistry:<ref name=ch09r60 /> |
* Mica-derived kaolinite characterizes fluvial/distributary-channel sands flushed by fresh water | * Mica-derived kaolinite characterizes fluvial/distributary-channel sands flushed by fresh water | ||
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==See also== | ==See also== | ||
| − | * [[ | + | * [[Sandstone porosity and permeability prediction]] |
* [[Sandstone diagenetic processes]] | * [[Sandstone diagenetic processes]] | ||
* [[Effect of composition and texture on sandstone diagenesis]] | * [[Effect of composition and texture on sandstone diagenesis]] | ||
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[[Category:Predicting the occurrence of oil and gas traps]] | [[Category:Predicting the occurrence of oil and gas traps]] | ||
[[Category:Predicting reservoir system quality and performance]] | [[Category:Predicting reservoir system quality and performance]] | ||
| + | [[Category:Treatise Handbook 3]] | ||
Latest revision as of 14:11, 6 April 2022
| Exploring for Oil and Gas Traps | |
| |
| Series | Treatise in Petroleum Geology |
|---|---|
| Part | Predicting the occurrence of oil and gas traps |
| Chapter | Predicting reservoir system quality and performance |
| Author | Dan J. Hartmann, Edward A. Beaumont |
| Link | Web page |
| Store | AAPG Store |
Depositional environment influences many aspects of sandstone diagenesis. The flow chart in Figure 1 shows the interrelationship of depositional environment with the many factors controlling sandstone diagenesis.
Figure 1 Flow chart showing the interrelationship of depositional environment with the many factors controlling sandstone diagenesis. After Stonecipher et al.[1]
Sediment texture and composition
Depositional environment affects sediment composition by determining the amount of reworking and sorting by size or hydraulic equivalence. Sediments that have a higher degree of reworking are more mechanically and chemically stable. The energy level of depositional environments affects sorting by size or hydraulic equivalence and consequently produces different detrital mineral suites.[2]
For example, different facies of the Wilcox Group along the Gulf Coast of Texas have different compositions that are independent of their source area.[2] Wilcox basal fluvial point bar sands are the coarsest and contain the highest proportion of nondisaggregated lithic fragments. Prodelta sands, deposited in a more distal setting, contain fine quartz, micas, and detrital clays that are products of disaggregation. Reworked sands, such as shoreline or tidal sands, are more quartzose.
Depositional pore-water chemistry
Depositional pore-water chemistry of a sandstone is a function of depositional environment. Marine sediments typically have alkaline pore water. Nonmarine sediments have pore water with a variety of chemistries. In nonmarine sediments deposited in conditions that were warm and wet, the pore water is initially either acidic or anoxic and has a high concentration of dissolved mineral species.[3]
Marine pore-water chemistry
Marine water is slightly alkaline. Little potential for chemical reaction exists between normal marine pore water and the common detrital minerals of sediments deposited in a marine environment. Therefore, diagenesis of marine sandstones results from a change in pore-water chemistry during burial or the reaction of less stable sediment with amorphous material.[3]
Marine diagenesis
Figure 2 Typical diagenetic pathways for marine sediments. Copyright: Burley et al.;[3] courtesy Blackwell Scientific.
The precipitation of cements in quartzarenites and subarkoses deposited in a marine environment tends to follow a predictable pattern beginning with clay authigenesis associated with quartz and feldspar overgrowths, followed by carbonate precipitation. Clay minerals form first because they precipitate more easily than quartz and feldspar overgrowths, which require more ordered crystal growth. Carbonate cement stops the further diagenesis of aluminosilicate minerals.
The diagram in Figure 2 summarizes typical diagenetic pathways for marine sediments.
Nonmarine pore-water chemistry and cements
Figure 3 Typical diagenetic pathways for warm and wet nonmarine sediments. Copyright: Burley et al.;[3] courtesy Blackwell Scientific.
Nonmarine pore-water chemistry falls into two climatic categories: (1) warm and wet or (2) hot and dry. The chemistry of pore waters formed in warm and wet conditions is usually acidic or anoxic with large concentrations of dissolved mineral species. The interaction of organic material with pore water is a critical factor with these waters. The depositional pore water of sediments deposited in hot and dry conditions is typically slightly alkaline and dilute.
The diagram in Figure 3 shows typical diagenetic pathways for warm and wet nonmarine sediments.
Cements
The table below, compiled from data by Thomas[4] shows the cements that generally characterize specific depositional environments.
| Environment | Facies | Cement |
|---|---|---|
| Eolian | Dune | Quartz overgrowths dominate; also clay coats |
| Interdune | Grain-coating clays; in areas that were alternately moist and dry anhydrite, dolomite, or calcite common | |
| Fluvial | Flood plain | Chlorite, illite, smectite, and mixed-layer clay |
| Channel | Calcite at base, grading up into calcite plus quartz, quartz plus clay minerals, and clays plus minor carbonate | |
| Nearshore marine | All | Carbonate minerals such as calcite or siderite; illite in sands deposited where fresh and marine water mix |
| Marine shelf | All | Calcite mainly; also dolomite, illite, chlorite rims, and quartz |
| Deep marine | All | Greater variety than other environments; cements include quartz, chlorite, calcite, illite, and occasional siderite or dolomite |
Diagenesis and depositional pore waters
In the Wilcox of the Texas Gulf Coast, certain minerals precipitate as a result of the influence of depositional pore-water chemistry:[1]
- Mica-derived kaolinite characterizes fluvial/distributary-channel sands flushed by fresh water
- Abundant siderite characterizes splay sands and lake sediments deposited in fresh, anoxic water
- Chlorite rims characterize marine sands flushed by saline pore water
- Glauconite or pyrite characterizes marine sediments deposited in reducing or mildly reducing conditions
- Illite characterizes shoreline sands deposited in the mixing zone where brackish water forms
- Chamosite characterizes distributary-mouth-bar sands rapidly deposited in the freshwater–marine water mixing zone
See also
- Sandstone porosity and permeability prediction
- Sandstone diagenetic processes
- Effect of composition and texture on sandstone diagenesis
- Hydrology and sandstone diagenesis
- Predicting sandstone reservoir porosity
- Predicting sandstone permeability from texture
- Estimating sandstone permeability from cuttings
References
- ↑ 1.0 1.1 Stonecipher, S. A., R. D. Winn, Jr., and M. G. Bishop, 1984, Diagenesis of the Frontier Formation, Moxa Arch: a function of sandstone geometry, texture and composition, and fluid flux, in D. A. McDonald, and R. C. Surdam eds., Clastic Diagenesis: AAPG Memoir 37, p. 289–316.
- ↑ 2.0 2.1 Stonecipher, S. A., and J. A. May, 1990, Facies controls on early diagenesis: Wilcox Group, Texas Gulf Coast, in D. Meshri and P. J. Ortoleva, eds., Prediction of Reservoir Quality Through Chemical Modeling, I: AAPG Memoir 49, p. 25–44.
- ↑ 3.0 3.1 3.2 3.3 Burley, S. D., J. D. Kantorowicz, and B. Waugh, 1985, Clastic diagenesis, in P. J. Brenchley, and B. P. J. Williams, eds., Sedimentology: Recent Developments and Applied Aspects: London, Blackwell Scientific Publications, p. 189–228.
- ↑ Thomas, R., 1983, An introduction to the thin section analysis of the diagenetic histories of clastic rocks, in I. Hutcheon, A. Oldershaw, and R. Thomas, eds., Clastic diagenesis: Canadian Society of Petroleum Geologists Short Course, University of Calgary, chapter 3, 56 p.
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