Influence of physiology and climate on δD of leaf wax n-alkanes from C3 and C4 grasses

Smith, Francesca A.; Freeman, Katherine H.

doi:10.1016/j.gca.2005.11.006

Cited by 340 publications

(347 citation statements)

References 69 publications

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“…Both controlled greenhouse experiments (14) and field experiments (19,20) support that the idea that the δ 2 H n-alkane values of grass leaf-wax n-alkanes reflect a continuous growth process. These studies show that the δ 2 H n-alkane values of grasses vary with the δ 2 H values of source and leaf water (14,19,20). This pattern supports the hypothesis that the δ 2 H n-alkane values of grass leaf waxes reflect the leaf-water environment during leaf expansion.…”

Section: In Deciduous Species δ 2 H Values Reflect Plant Environment mentioning

confidence: 55%

“…Differences in modeled precipitation δ 2 H values are not unexpected; however, mean annual precipitation δ 2 H values are used commonly to model leaf-wax δ 2 H values from plants (19,(33)(34)(35) and sediments (9,36). Often when mean annual precipitation δ 2 H values are used to calculate the apparent fractionation between the δ 2 H values of leaf wax and source waters, the resulting fractionation is smaller than expected (i.e., leaf waxes are more enriched in 2 H than predicted).…”

Section: In Deciduous Species δ 2 H Values Reflect Plant Environment mentioning

confidence: 99%

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Leaf-wax n -alkanes record the plant–water environment at leaf flush

Tipple

Berke

Doman

et al. 2013

Proc. Natl. Acad. Sci. U.S.A.

183

103

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Leaf-wax n-alkanes 2 H/ 1 H ratios are widely used as a proxy in climate reconstruction. Although the broad nature of the relationship between n-alkanes δ 2 H values and climate is appreciated, the quantitative details of the proxy remain elusive. To examine these details under natural environmental conditions, we studied a riparian broadleaf angiosperm species, Populus angustifolia, growing on water with a constant δ 2 H value and monitored the δ 2 H values of leaf-wax n-alkanes and of stem, leaf, stream, and atmospheric waters throughout the entire growing season. Here we found the δ 2 H values of leaf-wax n-alkanes recorded only a 2-wk period during leaf flush and did not vary for the 19 weeks thereafter when leaves remained active. We found δ 2 H values of leaf-wax n-alkanes of P. angustifolia record conditions earlier in the season rather than fully integrating the entire growing season. Using these data, we modeled precipitation δ 2 H values during the time of wax synthesis. We observed that the isotope ratios of this precipitation generally were 2 H-enriched compared with mean annual precipitation. This model provides a mechanistic basis of the often-observed 2 H-enrichment from the expected fractionation values in studies of broadleaf angiosperm leaf-wax δ 2 H. In addition, these findings may have implications for the spatial and temporal uses of n-alkane δ 2 H values in paleoapplications; when both plant community and growth form are known, this study allows the isolation of the precipitation dynamics of individual periods of the growing season.biomarkers | compound-specific isotope analysis | geographic information system | isoscape | stable isotopes S table isotopes serve as tracers and integrators of both environmental and physiological signals within plant materials. Terrestrial plant leaf waxes (i.e., n-alkanes, n-acids, and others) and their isotope ratios have attracted much interest as a higher plant-specific biomarker for paleoclimate reconstruction (1), because these compounds are easily identified and isolated from a variety of geologic materials and are relatively robust to geologic alteration (2). The environmental information recorded in hydrogen isotope ratios of leaf waxes have become a prevalent proxy to reconstruct ancient climates (3-5), mountain building events (6, 7), and floral transitions (8). However, critical questions related to the interpretation of ancient higher plant biomarkers remain unanswered, especially with respect to the extent of the leaf life cycle recorded by this proxy.Environmental and climate transect studies have shown that δ 2 H values of higher plant n-alkanes and environmental waters are correlated (9, 10), but temporal observations of δ 2 H values of n-alkanes have produced conflicting data on the nature of this relationship (11-15) that require clarification to elucidate how δ 2 H values of ancient n-alkanes can be interpreted. To reconcile these issues and to provide the critical constraints for climate reconstructions using δ 2 H values of n-alkanes, car...

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Section: In Deciduous Species δ 2 H Values Reflect Plant Environment mentioning

confidence: 55%

Section: In Deciduous Species δ 2 H Values Reflect Plant Environment mentioning

confidence: 99%

Leaf-wax n -alkanes record the plant–water environment at leaf flush

Tipple

Berke

Doman

et al. 2013

Proc. Natl. Acad. Sci. U.S.A.

183

103

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“…Overall, C 4 grasses are deuteriumdepleted by ∼ 20 ‰ relative to C 3 trees (McInerney et al, 2011) and deuterium-enriched by ∼ 20 ‰ relative to C 3 grasses (Smith and Freeman, 2006). However, the absolute variability of δ 13 C 31 is small (∼ 2 ‰) and would correspond to a vegetation shift between C 3 vs. C 4 plants of less than 20 %, when using the δ 13 C end-members of −35.2 ‰ for C 3 plants and −21.7 ‰ for C 4 plants (Castañeda et al, 2009).…”

Section: Plant-wax Provenance and Vegetation Sourcesmentioning

confidence: 97%

Hybrid insolation forcing of Pliocene monsoon dynamics in West Africa

2018

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Abstract. The Pliocene is regarded as a potential analogue for future climate with conditions generally warmer-thantoday and higher-than-preindustrial atmospheric CO 2 levels. Here we present the first orbitally resolved records of continental hydrology and vegetation changes from West Africa for two Pliocene time intervals (5.0-4.6 Ma, 3.6-3.0 Ma), which we compare with records from the last glacial cycle (Kuechler et al., 2013). Our results indicate that changes in local insolation alone are insufficient to explain the full degree of hydrologic variations. Generally two modes of interacting insolation forcings are observed: during eccentricity maxima, when precession was strong, the West African monsoon was driven by summer insolation; during eccentricity minima, when precession-driven variations in local insolation were minimal, obliquity-driven changes in the summer latitudinal insolation gradient became dominant. This hybrid monsoonal forcing concept explains orbitally controlled tropical climate changes, incorporating the forcing mechanism of latitudinal gradients for the Pliocene, which probably increased in importance during subsequent Northern Hemisphere glaciations.

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“…The isotopic fractionation between plant water and environmental water depends on physiological factors affecting water uptake, transport and evapotranspiration, considering aerial plants for this latter (Sessions et al, 2006;Smith and Freeman, 2006). The main isotopic fractionation occurs during lipid biosynthesis, depending on biosynthetic pathways (n-alkyl lipids versus isoprenoids for example) and compartmentalization of water use.…”

Section: Biological Factorsmentioning

confidence: 99%

Paleohydrological changes during the last deglaciation in Northern Brazil

Jacob

Huang

Disnar

et al. 2007

Quaternary Science Reviews

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We here report a reconstruction of hydrological balance variations in Northern Brazil for the last 20 ka deduced from the δD values of aquatic and land plant molecules extracted from the sediment infill of Lake Caçó. Our reconstructed precipitation, lake water isotope ratio and evaporation-evapotranspiration isotope effect allow us to obtain an estimate of moisture balance, and, to a lesser extent, precipitation amount and seasonality changes.

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Influence of physiology and climate on δD of leaf wax n-alkanes from C3 and C4 grasses

Cited by 340 publications

References 69 publications

Leaf-wax n -alkanes record the plant–water environment at leaf flush

Leaf-wax n -alkanes record the plant–water environment at leaf flush

Hybrid insolation forcing of Pliocene monsoon dynamics in West Africa

Paleohydrological changes during the last deglaciation in Northern Brazil

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