On the relationship between silica and carbonate diagenesis in deep-sea sediments

Hobert, Linda A.; Wetzel, Andreas

doi:10.1007/bf01829321

Cited by 11 publications

(8 citation statements)

References 24 publications

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“…In this depth interval, the chalk has an Oligocene age corresponding to 31-43 Ma (Kroenke et al, 1991), and an estimated temperature of 15-20°C. In line with the observations of Hobert & Wetzel (1989), the transition from opal-A to opal-CT is accompanied by a fall in specific surface of the sediment as measured by BET (Fig. 4).…”

Section: Silica and Silicatessupporting

confidence: 89%

“…A control of calcite cementation by silica was also reported by Hobert & Wetzel (1989). They studied deep-sea carbonates and found 'carbonate sediments containing chert (1) tend to be more indurated and display more advanced diagenetic alteration, regardless of subbottom depth'.…”

Section: Calcite Cementation -Role Of Silicamentioning

confidence: 71%

“…Heald, 1955;Simpson, 1985;Lind, 1993a;Sheldon et al, 2003;Safaricz & Davison, 2005). It also remains unclear how diagenetically controlled changes in the mineralogy of silicates in the chalk influence changes in the dominating carbonate phase (Baker et al, 1980;Hobert & Wetzel, 1989). Finally presence of hydrocarbons may have an influence on the diagenetic process (Scholle, 1977).…”

Section: Introductionmentioning

confidence: 99%

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Stylolites, porosity, depositional texture, and silicates in chalk facies sediments. Ontong Java Plateau – Gorm and Tyra fields, North Sea

Fabricius¹,

Borre²

2006

Sedimentology

101

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Comparison of chalk on the Ontong Java Plateau and chalk in the Central North Sea indicates that, whereas pressure dissolution is controlled by effective burial stress, pore‐filling cementation is controlled by temperature. Effective burial stress is caused by the weight of all overlying water and sediments as counteracted by the pressure in the pore fluid, so the regional overpressure in the Central North Sea is one reason why the two localities have different relationships between temperature and effective burial stress. In the chalk of the Ontong Java Plateau the onset of calcite‐silicate pressure dissolution around 490 m below sea floor (bsf) corresponds to an interval of waning porosity‐decline, and even the occurrence of proper stylolites from 830 m bsf is accompanied by only minor porosity reduction. Because opal is present, the pore‐water is relatively rich in Si which through the formation of Ca–silica complexes causes an apparent super‐saturation of Ca and retards cementation. The onset of massive pore‐filling cementation at 1100 m bsf may be controlled by the temperature‐dependent transition from opal‐CT to quartz. In the stylolite‐bearing chalk of two wells in the Gorm and Tyra fields, the nannofossil matrix shows recrystallization but only minor pore‐filling cement, whereas microfossils are cemented. Cementation in Gorm and Tyra is thus partial and has apparently not been retarded by opal‐controlled pore‐water. A possible explanation is that, due to the relatively high temperature, silica has equilibrated to quartz before the onset of pressure dissolution and thus, in this case, dissolution and precipitation of calcite have no lag. This temperature versus effective burial stress induced difference in diagenetic history is of particular relevance when exploring for hydrocarbons in normally pressured chalk, while most experience has been accumulated in the over‐pressured chalk of the central North Sea.

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Section: Silica and Silicatessupporting

confidence: 89%

Section: Calcite Cementation -Role Of Silicamentioning

confidence: 71%

Section: Introductionmentioning

confidence: 99%

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Stylolites, porosity, depositional texture, and silicates in chalk facies sediments. Ontong Java Plateau – Gorm and Tyra fields, North Sea

Fabricius¹,

Borre²

2006

Sedimentology

101

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“…Several authors have suggested that silicate content in chalk may inhibit or delay calcite recrystallization and cement formation (Hobert & Wetzel, ; Tucker & Wright, ; Zuddas & Mucci, ; Røgen & Fabricius, ; Fabricius, ; Arribas et al ., ; Fabricius & Borre, ; Mallon & Swarbrick, ; Alam et al ., ). Others have indicated that high clay content (10 to 20%) promotes pressure‐dissolution between micritic grains (Fabricius & Borre, ; Aharonov & Katsman, ; Deville de Periere et al ., ).…”

Section: Discussionmentioning

confidence: 99%

Classifying chalk microtextures: Sedimentary versus diagenetic origin (Cenomanian–Santonian, Paris Basin, France)

et al. 2019

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Microtexture describes the type of particles and their arrangement in matrix samples at scanning electron microscopy scale. Although a microtexture classification exists for micritic limestone, it cannot be directly applied to chalk. This study therefore proposes a classification of chalk microtextures and discusses the origin of microtexture variability. Chalk was sampled at thirteen spatio-temporal locations along the coastline of northern France (Cenomanian-Santonian). Four criteria are defined to describe, characterize and determine chalk matrix microtexture: (i) mineralogical content; (ii) biogenic fraction; (iii) micritic fraction; and (iv) cement fraction. From these criteria, two major groups are defined: Pure Chalk Microtexture Group, with seven classes, and Impure Chalk Microtexture Group, divided into two subgroups: Argillaceous Microtexture with four classes and Siliceous Microtexture with two classes. Microtexture variability is related both to initial sedimentation and to diagenesis. Sedimentological conditions (for example, climate and distance from shore) affect chalk composition (carbonate content and type of insoluble particles), thus influencing microtexture. Changes in Pure Chalk Microtexture are the result of increasing diagenetic intensity. This classification can also be used to characterize the microtexture of subsurface chalk reservoirs. Reservoir quality depends on the petrophysical and mechanical properties of reservoir rocks, which can be better understood by exploring their sedimentary and diagenetic history, revealed by the study of chalk microtexture variability.

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“…However, evidence suggests that loss and replacement of OM may be substantial within floodplains, estuarine and deltaic systems (Galy et al, 2008;Keil et al, 1997). Estimates of MSA in marine sediments are complicated by the production and deposition of biogenic carbonate and opal (Hobert and Wetzel, 1989). However, sediment trap data from the central BoB suggest 630 that modern-day carbonate and opal fluxes to BoB are relatively low (0.03 -3.1 g/m 2 per year; Sarin et al, 1979).…”

Section: Linkages Between Godavari Drainage Basin and Marine Sedimentmentioning

confidence: 99%

Reconciling drainage and receiving basin signatures of the Godavari River system

Usman¹,

Kirkels²,

Zwart³

et al. 2018

Preprint

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Abstract. The modern-day Godavari River transports large amounts of sediment (170 Tg per year) and terrestrial organic carbon (OC terr ; 1.5 Tg per year) from peninsular India to the Bay of Bengal. The flux and nature of OC terr is considered to have varied in response to past climate and human forcing. In order to delineate the provenance and nature of organic matter (OM) exported 5 by the fluvial system and establish links to sedimentary records accumulating on its adjacent continental margin, the stable and radiogenic isotopic composition of bulk OC, abundance and distribution of long-chain fatty acids (LCFA), sedimentological properties (e.g. grain size, mineral surface area etc.) of fluvial (riverbed and riverbank) sediments and soils from the Godavari 10 basin were analysed and these characteristics were compared to those of a sediment core retrieved from the continental slope depocenter. Results show that river sediments from the upper catchment exhibit higher total organic carbon (TOC) contents than those from the lower part of the basin. The general relationship between TOC and sedimentological parameters (i.e., 15 mineral-specific surface area and grain size) of the sediments suggests that sediment mineralogy, largely driven by provenance, plays an important role in the stabilization of OM during transport along the river axis, and in preservation of OM exported by the Godavari to the Bay of Bengal. The stable carbon isotopic (δ 13 C) characteristics of river sediments and soils indicate that 20

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On the relationship between silica and carbonate diagenesis in deep-sea sediments

Cited by 11 publications

References 24 publications

Stylolites, porosity, depositional texture, and silicates in chalk facies sediments. Ontong Java Plateau – Gorm and Tyra fields, North Sea

Stylolites, porosity, depositional texture, and silicates in chalk facies sediments. Ontong Java Plateau – Gorm and Tyra fields, North Sea

Classifying chalk microtextures: Sedimentary versus diagenetic origin (Cenomanian–Santonian, Paris Basin, France)

Reconciling drainage and receiving basin signatures of the Godavari River system

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