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Zementbildung
Christian Björn Muñoz GuerreroAlexander KellermeierYunsang JoTong Zhang
25. April 2018
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Gliederung
1. Definition Zementation& Unterschied Matrix/Zement2. Quarz-Zementation3. Feldspat4. Tonminerale5. Karbonat6. Phosphat7. Sulfat/Sulfid8. Eisenoxid
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Definition Zement/Zementation
• Zement: Verfüllung des Porenraums
zwischen den Sedimentpartikeln mit
einer authigenen Mineralbildung welche
durch die Diagenese induziert wird
(Kalzit, SiO2,…)
• Zementation: Ausfällung und/oder
Kristallisation von Mineralen
(diagenetische Veränderung)
Ausfällung zwischen den Partikeln bewirkt Porenraumverkleinerung
Grotzinger & Jordan 2010 3
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Zement & Matrix
• Bildet in der Regel die Grundmasse eines
Sedimentgesteins
• Unterschied:
• Zement (postsedimentär): kristallin
• Matrix (synsedimentär): feinkörniges
sedimentäres Material
Zusätzlich: Unterschiede in Bildungszeit, -ort, -merkmale und Gefüge (direkter Vergleich in Füchtbauer (1988)
Earth Science Australia, http://earthsci.org
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Zement - Quarz
Stylolitisierung
Rekristallisationsprozesse
Feldspat-Lösung
5Oelkers et al.,1996
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Zement ‐ Quarz
Mechanismen/Raten von Qz-Zementation verstehen für die Quantifizierung von Wechseln bei physikalischen Eigenschaften während der Versenkung
Rate der Qz-Zementation als Funktion der Zeit, Temperatur (T) und Qz-Oberfläche
Analysen mittels Isotopenverteilung δ18O im Bezug auf die Temperatur
Harwood et al. 2013
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Zement - Feldspat
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Zemente können Aussagen über dasAblagerungsmilieu wiedergeben; Tendenz:Kalifeldspat: kontinental, arid(Füchtbauer, 1974; Houareau,1974; Waugh, 1978)Albit: marin (Almon et al., 1976)
Vorkommen: Im Bereich der Diagenese und bei schwachen Metamorphosegraden (abhängig von der Gesteinszusammensetzung(Füchtbauer, 1988)
1) Lösungsprozesse: 4 KAlSi3O8+ 4 H2OAl4(OH)8Si4O10+ 2K2O+ 8SiO2
2) Albitisierung: KAlSi3O8 + Na+NaAlSi3O8+K+
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ementation of Clay mineral:
Cement in sandstone reservoir is dominated by
ceous and carbonate cement,
h minor amounts of clay minerals and sulfides.
Kaolinite (Al2Si2O5(OH)4)
early diagenetic (eogenetic) origin
Chlorite (Fe-Mg)5Al2Si3O10(OH)8)
burial diagenetic (mesogenetic) origin
Illite (KAl3Si3O10(OH)2)
burial diagenetic (mesogenetic) origin
nerally, clay minerals are dominated by kaolinite and chlorite, followed by illite and mixed-layer
e/ smectite. With the increase of the buried depth of sandstone, the content of illite is increasing.
Wüstefeld, P, 2
Near-surface diagenesis
Ca. 70℃
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Kaolinite (Al2Si2O5(OH)4)
•Early diagenetic (eogenetic) origin
•Low temperature/ shallow depth
•as fillings in primary pores, secondary
pores in the shapes of books and worms,
with the throat in the local partProcess:
Kaolinite is precipitated after most of
the feldspar has been dissolved
Major controlling Parameter:Abundance of feldspars, effective meteoric
water flux and sea-water
Depositional facies: marine and fluvial sandstones
R. H. Worden, 2003, M. J. Wilson, 20
SEM image showing oldest cement in the sandstones consisting of intergrown kaolinite (orange) and calcite (blue)
Scanning electron microscope (SEM) micrographs illustrating Well-ordered kaolinite in discrete booklets
ESEM images showing typical cement habits and dissolution of He8 sandstones; Book-like kaolinite occludes pore and pore throat
b
c d
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Kaolinite (Al2Si2O5(OH)4)• Process:
Kaolinite is precipitated after most of
the feldspar has been dissolved by
chemical weathering during early diagenesis
Nedkvitne and Bjørlykke, 1992; Bjørlykke, 2010
A2K(Na)AlSi3O8+2H+9H2O=FeldsparAl2Si2O5(OH)4+4H4SiO4+2K(2Na)Kaolinite
Precondition for the formation of clay minerals:
1)Silicates provide a source of material for
authigenic clays
2)Silicate dissolution increases the
microporosity (secondary porosity) of
rock
A
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Kaolinite (Al2Si2O5(OH)4)• Process:
Kaolinite is precipitated after most of
the feldspar has been dissolved by
chemical weathering during early diagenesis
Nedkvitne and Bjørlykke, 1992; Bjørlykke, 2010
B
2K(Na)AlSi3O8+2H+9H2O=FeldsparAl2Si2O5(OH)4+4H4SiO4+2K(2Na)Kaolinite
Precondition for the formation of clay minerals:
1)Silicates provide a source of material for
authigenic clays
2)Silicate dissolution increases the
microporosity (secondary porosity) of
rock
B
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Kaolinite (Al2Si2O5(OH)4)
• Major controlling parameter:
1. Type and amount of water
Fresh water (low pH, low ionic strength)
Marine (high pH, high ionic strength)
2. Water influx versus evaporation rate
3. Temperature
4. Organic matter component etc.
“Saturated”A B C
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Kaolinite (Al2Si2O5(OH)4)
The role of depositional environment on clay mineral patterns in sandstones will be divided between subaerial and marine syste
Continental environments will be split between warm and wet versus arid.
• Major controlling parameter:
1. Type and amount of water
Fresh water (low pH, low ionic strength)
Marine (high pH, high ionic strength)
2. Water influx versus evaporation rate
3. Temperature
4. Organic matter componant etc.
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Kaolinite (Al2Si2O5(OH)4)• Depositional environments: Cont. environment (warm and wet)
Alluvial-fluvial environments (alluvial fans, fluvial braided streams, fluvial meandering streams)
• Pore waters in humid, warm (subtropic
to temperate) environments are dilute
Low ionic concentrations in pore
waters close to main channel
• Abundance of organic matter that
undergoes bacterially mediated decay
(Berner, 1980)
Organic (humic) acids in abandoned
channels
Encouraging extreme feldspar
weathering
R. H. Worden, 2003
Stagnate -> saturated ions
Organic acids
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Kaolinite (Al2Si2O5(OH)4)• Depositional environments: Cont. environment (arid)
Prograding fluvial deltas (prograding into a playa=dry delta)
• Clay eodiagenesis in arid eogenetic
environment
• In the unsaturated zone of aquifers,
clay infiltration occurs,
if percolating waters contain
suspended clay menerals
(Moraes & de Ros, 1990)
When ground water evaporation
exceeds the rate of percolation =>
leaving the suspended clay mineral
coated on sand grains
Kaolinite may form from detrital feldspars i
the aquifer if the groundwater is flowing
and being recharged.R. H. Worden, 2003
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Kaolinite (Al2Si2O5(OH)4)• Depositional environments: Cont. environment (arid)
Prograding fluvial deltas (prograding into a playa=dry delta)
• Clay eodiagenesis in arid eogenetic
environment
• In the unsaturated zone of aquifers,
clay infiltration occurs,
if percolating waters contain
suspended clay menerals
(Moraes & de Ros, 1990)
When ground water evaporation
exceeds the rate of percolation =>
leaving the suspended clay mineral
coated on sand grains
Kaolinite may form from detrital feldspars i
the aquifer if the groundwater is flowing
and being recharged.
(A, B & C) SEM images of coated sand grain from sample B10 65-70 cm. (D) EDX spectra of coat indicating the presence of kaolinite.Patrick J. Dowey, 2017
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Karbonatzemente
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Karbonatzemente
• Die meisten Kabonatzemente entstehen während der Diagenese
• Karbonatzemente sind oft an der Verfüllung des Porenraums von Sandsteinen beteiligt
• Karbonatzemente typischerweise in Quartz-Areniten vertreten
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Aragonit, Kalzit
Tucker/Wright,1996
Tucker/Wright,1996
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Tucker/Wright, 1996
High‐/Low Mg Kalzit und Aragonit1 Kallkspatzement in kalten, Tiefwasser-Sedimenten, Sedimenten in geringen Breitengraden und temperierten Flachwasser-Sedimenten2 high-Mg Kalzitzement in Riffen (selten)3 high-Mg Kalzitzement in Riffen und Kalksanden 4 Aragonitzement in Riffen und Kalksanden 5 low-Mg Kalkspatzement in meteorischer Umgebung6 low-Mg Kalzit in Speleothemen und Travertinen7 Aragonit in Speleothemen (selten)
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Dolomitisierung
Tucker/Wright,1996
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Tucker/Wright, 1996
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Pettijohn, 198723
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Tucker/Wright, 1996
Keine allgemeine Ausfällungsabfolge bestimmbarAusfällung der unterschiedlichen Karbonattypen abhängig vom Ablagerungsmilieu•Offene oder geschlossene Systeme•Ausgangszusammensetzung und Stabilität der einzelnen Komponenten•Salinität•Mg/Ca-Verhältnis•pH-Wert •Eh-Wert•T-P-Bedingungen•Zeit
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Bildung von Zementen
Phosphat, Sulfate und Sulfide bzw Eisenoxide
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PhosphatZement
K. P. KRAJEWSKI 1984
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Entstehung
K. P. KRAJEWSKI 1984
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Phosphate Cement fabrics
K. P. KRAJEWSKI 1984
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Zusammenfassung• Vorkommen von Phosphat‐Zementen‐feinkörniges marines Sediment‐Ein früh diagenetisches marines Phänomen‐Hohe Phosphatkonzentration im Sediment‐organisches Material als Phosphatquelle nötig
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Sulfate und Sulfide Zement
• Gips CaSO4*H20• Anhydrit CaSO4
• Baryt BaSO4
• ______________________• Pyrit FeS2 (kubisch)• Markasit FeS2 (orthorhomb)
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Anhydrit‐Zemente im Persischen Golf
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Anhydrit‐Zemente im Persischen Golf
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Eisenoxid Zement
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Nielsen et al., 2014
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Chemismus• Hematite:2Fe2+(aq) + 0,5 O2(g) + 2H2O(l) = Fe2O3(s) + 4H+
(aq)
goethite:• 2Fe2+(aq) + 0,5 O2(g) + 3H2O(l) = 2FeO(OH)(s) +4H+
(aq)
dehydration of goethite:2FeO(OH)(s) = Fe2O3(s) + H2O(l)
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ZusammenfassungMineralische Porenwässer gelangen in die Porenräume des Lockersediments undfällen dort aus. (Die Porosität wird dadurch verringert)Die kontrollierte Parameter für die Bildung von Zement sind chemisch undphysikalisch. (z.B. Druck, Temperatur, Porosität, Mineralzusammensetzung vonKomponent, pH‐Wert, Eh‐Wert usw.)Zemente bestehen meist aus Kalziumkarbonat (Kalzit, Dolomit) oder Siliziumdioxid(Quarz, Feldspat,Kaolinit), seltener aus anderen Mineralen.Es gibt häufig zwei oder mehr Generationen von Zement. Um die verschiedenenGenerationen von Zemente oder Sammelkristallisation der Matrix zu unterscheidenist nicht nur lichtmikroskopische Untersuchung sondern auch Kathodolumineszenz‐Mikroskopie erforderlich.
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Literatur• Pettijohn, F.J.;Potter,P.E.;Siever,R., 1987: Sand and Sandstone,Springer Verlag, 2. Auflage
• Tucker, M.E.;Wright, V.P.,1996: Carbonate Sedimentology, Backwell Science Ltd
• Füchtbauer, H., 1988. Sediment-Petrologie, Teil 2: Sedimente und Sedimentgesteine, Schweizerbart, 4. Auflage. S.165, 167f,174f, 177f, 376, 421ff
• Füchtbauer,H.; Müller,1977:Sediment-Petrologie, Teil 2-Sedimente und Sedimentgesteine, Schweizerbart´sche Verlagsbuchhandlung, 3. Auflage
• Elbracht,J., 2002: Karbonatische Zementation pleistozäner Lockersedimente NW-Deutschlands, Dissertation Universität Hannover
• R. H. Worden and S. Morad., 2003. clay minerals in sandstones: controls on formation, distribution and evolution
• Meng Wang, Hongming Tang and Feng Zhao., 2017. controlling factor analysis and prediction of the quality of tight sandstone reservoir: A case study of the He8 member in the eastern Sulige GasField, Ordos Basin, China. Journal of Natural Gas Science and Engineering 46 (2017) 680-698
• S. Morad, Khalid Al-Ramadan, J. M. Ketzer, and L. F. De Ros., 2010. the impact of diagenesis on the heterogeneity of sandstone reservoirs: A review of the role of depositional facies and sequence stratigraphy. AAPG Bulletin, v. 94, no. 8 (August 2010), pp. 1267–1309
• Dowey, Patrick J., Worden, Richard H., Utley, James, Hodgson, David M., 2007. Sedimentary controls on modern sand grain coat formation, Sedimentary Geology.
• Patrick Wüstefeld, Ulrike Hilse, Bastian Koehrer, Dirk Adelmann, Christoph Hilgers., 2017. Critical evaluation of an Upper Carboniferous tight gas sandstone reservoir analog: Diagenesis and petrophysical aspects
• Rahimpour-Bonab H., Esrafili-Dizaji B., Tavakoli V. (2010): Dolomitization and Anhydrite Precipitation in Permo-Triassic Carbonates at the South Pars Gasfield, Offshore Iran: Controls on Reservoir Quality. Journal of Petroleum Geology, Vol. 33 (I), Seite 43-66.
• Krajewski, K. P. (1984), Early diagenetic phosphate cements in the Albian condensed glauconitic limestone of the Tatra Mountains, Western Carpathians Sedimentology Volume 31, Issue 4, pages 443–470, August 1984
• Nielsen, G.B., Chan, M.A., and Bowen, B.B. (2014): IRON-RICH HORIZONS IN THE JURASSIC NAVAJO SANDSTONE,SOUTHWESTERN UTAH: PROGRESSIVE CEMENTATION AND PERMEABILITY INVERSION. UGA Publication 43 (2014)
• Harwood, J., 2013, Quartz Cementation History of Sandstones Revealed By High-Resolution Sims Oxygen IsotopeAnalysis: Journal of Sedimentary Research, v.83(7), p.522-530
• Grotzinger, J., Jordan, T., 2010. Understanding Earth (6. Auflage). W. H. Freeman and Company, New York
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