2013
DOI: 10.1016/j.palaeo.2013.09.020
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Oxygen and hydrogen isotope compositions of paleosol phyllosilicates: Differential burial histories and determination of Middle–Late Pennsylvanian low-latitude terrestrial paleotemperatures

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Cited by 22 publications
(21 citation statements)
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“…The d 18 O value of the calcite formed during the final stage of meteoric exposure is 25.6%, which likely formed from meteoric waters with d 18 O SMOW of 23% to 24%, assuming precipitation at mean annual temperatures typical of expected values for an equatorial setting and accounting for possible secular shifts in the d 18 O of marine water (Lohmann and Walker 1989). This estimate is compatible with values calculated from paleosols of middle-late Pennsylvanian age (Rosenau and Tabor 2013). If it is assumed that this meteoric water remained as the interstitial fluids responsible for burial diagenesis, the difference (D 18 O) in d 18 O composition between the meteoric and burial calcites can be used to calculate the increase in fluid temperature.…”
Section: Depositional History Of the Holder Formation Inferred From Psupporting
confidence: 81%
“…The d 18 O value of the calcite formed during the final stage of meteoric exposure is 25.6%, which likely formed from meteoric waters with d 18 O SMOW of 23% to 24%, assuming precipitation at mean annual temperatures typical of expected values for an equatorial setting and accounting for possible secular shifts in the d 18 O of marine water (Lohmann and Walker 1989). This estimate is compatible with values calculated from paleosols of middle-late Pennsylvanian age (Rosenau and Tabor 2013). If it is assumed that this meteoric water remained as the interstitial fluids responsible for burial diagenesis, the difference (D 18 O) in d 18 O composition between the meteoric and burial calcites can be used to calculate the increase in fluid temperature.…”
Section: Depositional History Of the Holder Formation Inferred From Psupporting
confidence: 81%
“…It is estimated that the maximum burial depth of most Pennsylvanian strata did not exceed , 1500 m (equivalent to eroded post-Carboniferous strata), and except for perhaps a brief duration in deeper, southern portions of the basin, most strata did not experience burial temperatures in excess of 100 uC (Harris 1979;Grathoff et al 2001). This relatively mild burial history is supported by recent crystallization temperature estimates from paleosol phyllosilicates across the basin (Rosenau and Tabor 2013). Considering the relatively mild burial history of these fossils, the Illinois Basin conodont apatite d 18 O values reported herein are considered to preserve d 18 O values acquired by the conodonts during the Pennsylvanian.…”
Section: Assessing Diagenesismentioning
confidence: 57%
“…be related to surface temperatures (Tabor & Montañez 2005, Tabor 2007, Yapp 2008. However, there is a disconnect between reported oxygen and hydrogen isotope fractionation equations for phyllosilicates (Delgado & Reyes 1996, Sheppard & Gilg 1996 and those for paleosol clay assemblages, which are typically complex mixtures of kaolinite, smectite, illite, and mixed-layer illite-smectite (e.g., Rosenau & Tabor 2013). Application of experimentally derived fractionation factors for pure smectite to phyllosilicate assemblages that also include kaolinite and illite yields overestimates of actual crystallization temperatures (Myers et al 2012b).…”
Section: Principles Of Stable Isotope Geochemistrymentioning
confidence: 99%
“…Application of experimentally derived fractionation factors for pure smectite to phyllosilicate assemblages that also include kaolinite and illite yields overestimates of actual crystallization temperatures (Myers et al 2012b). X-ray diffraction analysis of mineral composition, in conjunction with elemental analysis, allows calculation of unique fractionation factors for each clay assemblage (Rosenau & Tabor 2013). Although this in-depth approach may not be appropriate for every paleosol-based paleoclimate reconstruction, it represents a significant improvement in the accuracy of paleotemperature estimates derived from pedogenic phyllosilicates.…”
Section: Principles Of Stable Isotope Geochemistrymentioning
confidence: 99%