Clay mineralogy, organic carbon burial, and redox evolution in Proterozoic oceans

Tosca, Nicholas J.; Johnston, David T.; Mushegian, Alexandra A.; Rothman, Daniel H.; Summons, Roger E.; Knoll, Andrew H.

doi:10.1016/j.gca.2009.12.001

Cited by 97 publications

(42 citation statements)

References 54 publications

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“…Pro gres sive chem i cal weath er ing leaches and re moves the sol u ble el e ments (Ca, Na, Mg and fi nally K) rel a tive to Al and, in some cases, Fe and Ti (e.g., Nesbitt and Young, 1982;Fedo et al, 1995Fedo et al, , 1997Tosca et al, 2010). This re flects the de crease in abun dance of both non-clay sil i cate min er als (plagioclases, K-feld spars) and compositionally im mature clay min er als such as smectite (cf.…”

Section: General Palaeoenvironmental and Palaeoclimatic Remarksmentioning

confidence: 99%

Climatic disaster at the Triassic-Jurassic boundary - a clay minerals and major elements record from the Polish Basin

Brański

2014

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1 Pol ish Geo log i cal In sti tute -Na tional Re search In sti tute, Rakowiecka 4, 00-975 Warszawa, Po land Brañski, P., 2014. Cli ma tic di sas ter at the Tri as sic-Ju ras sic bound ary -a clay min er als and ma jor el e ments re cord from the Pol ish Ba sin. Geo log i cal Quar terly, 58 (2): 291-310, doi: 10.7306/gq.1161The Tri as sic-Ju ras sic bound ary in ter val (ca. 201 Ma) was a time of sud den global en vi ron men tal changes trig gered by Pangea breakup and Cen tral At lan tic Mag matic Prov ince de vel op ment. The bulk-rock min er al ogy, clay min er al ogy and major el e ment geo chem is try of 87 con ti nen tal mudrock sam ples col lected from four bore hole cores yield in for ma tion on Rhaetian-ear li est Hettangian palaeoclimatic changes in the Pol ish Ba sin. Dur ing the Rhaetian, smectite pre pon der ance was re placed by kaolinite and illite dom i na tion. This fun da men tal shift in clay min eral as sem blages (sup ported by ma jor el ement data) in di cates very sig nif i cant change in cli mate hu mid ity. More over, some beds in the Zagaje For ma tion (Up per Rhaetian-Lower Hettangian) are par tic u larly rich in kaolinite in di cat ing ex treme chem i cal weath er ing in hu mid-sub trop i cal to trop i cal cli mate ep i sodes in the af ter math of pow er ful warm ing and abun dant rain fall. Im por tantly, the first dis tinct kaolinite en rich ment ap pears al ready in the Lower Rhaetian Wielichowo Beds. In ad di tion, abrupt and ep i sodic shifts in the kaolinite-illite ra tio and in val ues of weath er ing in di ces point to pro found cli mate de sta bi li sa tion and a se quence of fre quent, cat a strophic cli ma tic re ver sals in the Late Rhaetian and at the Tri as sic-Ju ras sic bound ary. These re sults are gen er ally consis tent with car bon iso tope re cords in sec tions world wide.Key words: Tri as sic-Ju ras sic bound ary, clay min er als, ma jor el e ments, weath er ing re gime, palaeoclimatic shifts, Pol ish Ba sin.

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Section: General Palaeoenvironmental and Palaeoclimatic Remarksmentioning

confidence: 99%

Climatic disaster at the Triassic-Jurassic boundary - a clay minerals and major elements record from the Polish Basin

Brański

2014

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“…Without known biological processes to catalyze its removal, Precambrian seawater was characterized by much higher concentrations of Si (Table 2), perhaps close to amorphous silica saturation (Siever, 1991(Siever, , 1992. Some silica must have been incorporated into clays formed authigenically within sediments (e.g., Tosca et al, 2010). Much, however, left the oceans as precipitates during evaporation of seawater and is preserved primarily as early diagenetic cherts in shallow water carbonate successions (Siever, 1992).…”

Section: Silica Cycling and Si Isotopes In Precambrian Oceansmentioning

confidence: 99%

Si isotope variability in Proterozoic cherts

Chakrabarti

Knoll

Jacobsen

et al. 2012

Geochimica et Cosmochimica Acta

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We report Si-isotopic compositions of 75 sedimentologically and petrographically characterized chert samples with ages ranging from $2600 to 750 Ma using multi-collector inductively coupled plasma mass spectrometry. d 30 Si values of the cherts analyzed in this study show a $7& range, from À4.29 to +2.85. This variability can be explained in part by (1) simple mixing of silica derived from continental (higher d 30 Si) and hydrothermal (lower d 30 Si) sources, (2) multiple mechanisms of silica precipitation and (3) Rayleigh-type fractionations within pore waters of individual basins.We observe $3& variation in peritidal cherts from a single Neoproterozoic sedimentary basin (Spitsbergen). This variation can be explained by Rayleigh-type fractionation during precipitation from silica-saturated porewaters. In some samples, postdissolution and reprecipitation of silica could have added to this effect. Our data also indicate that peritidal cherts are enriched in the heavier isotopes of Si whereas basinal cherts associated with banded iron formations (BIF) show lower d 30 Si. This difference could partly be due to Si being derived from hydrothermal sources in BIFs. We postulate that the difference in d 30 Si between non-BIF and BIF cherts is consistent with the contrasting genesis of these deposits. Low d 30 Si in BIF is consistent with laboratory experiments showing that silica adsorbed onto Fe-hydroxide particles preferentially incorporates lighter Si isotopes.Despite large intrabasinal variation and environmental differences, the data show a clear pattern of secular variation. Low d 30 Si in Archean cherts is consistent with a dominantly hydrothermal source of silica to the oceans at that time. The monotonically increasing d 30 Si from 3.8 to 1.5 Ga appears to reflect a general increase in continental versus hydrothermal sources of Si in seawater, as well as the preferential removal of lighter Si isotopes during silica precipitation in iron-associated cherts from silica-saturated seawater. The highest d 30 Si values are observed in 1.5 Ga peritidal cherts; in part, these enriched values could reflect increasing sequestration of light silica during soil-forming processes, thus, delivering relatively heavy dissolved silica to the oceans from continental sources. The causes behind the reversal in trend towards lower d 30 Si in cherts younger than 1.5 Ga old are less clear. Cherts deposited 1800-1900 Ma are especially low d 30 Si, a possible indication of transiently strong hydrothermal input at this time.

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“…Physical shielding in nanometer-scale pores is one of the mechanisms responsible for the preservation of organic matter on minerals (Alexander, 2000;Hedges and Oades, 1997;Nelson et al, 1999;Tosca et al, 2010). As the diameters of the smallest microorganisms (bacteria) in soils, sediments, and rocks are larger than 200 nm (NRC, 1999), they cannot directly access the organic contaminants sorbed in these tiny pores.…”

Section: Inhibition On Biodegradationmentioning

confidence: 99%

“…It has been observed that silicate and calcium carbonate biominerals and aluminosilicates in marine environment play an important role in protecting organic carbons, such as amino acids and proteins, from hydrolytic enzymes throughout the water column and surface sediments, leading to their non-selective preservation (Hedges et al, 2001;Ingalls et al, 2003;Mayer, 1994a;Ransom et al, 1998;Tosca et al, 2010). Micropores and mesopores in soil minerals have a similar role in the preservation of soil organic carbon (SOC) (Knicker, 2004;Krull et al, 2003;Mayer, 1994b;Mayer et al, 2004).…”

Section: Inhibition On Biodegradationmentioning

confidence: 99%

“…Among the mineral components in soils and sediments, clay minerals, particularly expandable minerals (vermiculite and smectite), whose interlayer space is highly expansible, appear to play the most important role in retaining organic compounds (Cheng and Reinhard, 2006b;Golchin et al, 1994;Hedges and Keil, 1995;Hundal et al, 2001;Keil et al, 1994;Mayer, 1994a,b;Hedges and Oades, 1997;Ransom et al, 1998;Riley et al, 2010;Tisdall and Oades, 1982;Tosca et al, 2010;Wang and Lee, 1993;Wu and Laird, 2002). More information on the chemical properties, textural arrangement, and surface characteristics of the dominant high surface area-to-volume minerals in marine sediments and soils and their interactions with organic matter is required to fully understand the mechanisms causing preservation of the organic carbons (Ransom et al, 1998;Tosca et al, 2010). Nonetheless, with the size exclusion effect, micropores and mesopores formed from stacking of mineral particles and those presented within the mineral particles in porous geological media could lead to reduction in bioavailability and biodegradation rates of organic contaminants and organic carbons.…”

Section: Inhibition On Biodegradationmentioning

confidence: 99%

See 1 more Smart Citation

Impact of mineral micropores on transport and fate of organic contaminants: A review

Cheng

2012

Journal of Contaminant Hydrology

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Clay mineralogy, organic carbon burial, and redox evolution in Proterozoic oceans

Cited by 97 publications

References 54 publications

Climatic disaster at the Triassic-Jurassic boundary - a clay minerals and major elements record from the Polish Basin

Climatic disaster at the Triassic-Jurassic boundary - a clay minerals and major elements record from the Polish Basin

Si isotope variability in Proterozoic cherts

Impact of mineral micropores on transport and fate of organic contaminants: A review

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