High-resolution record of Northern Hemisphere climate extending into the last interglacial period

,

doi:10.1038/nature02805

Cited by 2,597 publications

(568 citation statements)

References 53 publications

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“…These appear to be similar to the weak summer monsoon signals seen in the Hulu cave speleothems (Wang et al, 2001), the Yuanbao Loess profile , records of total reflectance (L ⁄ ) from the Arabian sea (Deplazes et al, 2013(Deplazes et al, , 2014, the Sanxing stalagmite d 18 O record (Jiang et al, 2014), and various cold event signals in Greenland ice cores (Andersen et al, 2004;Svensson et al, 2008) (Fig. 6).…”

Section: Synchronous Long-term Changes In Ism and Easm And Abrupt CLsupporting

confidence: 58%

Evolution of the Indian summer monsoon during the interval 32.7–11.4cal. ka BP: Evidence from the Baoxiu peat, Yunnan, southwest China

Huang

Wei

et al. 2016

Journal of Asian Earth Sciences

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Section: Synchronous Long-term Changes In Ism and Easm And Abrupt CLsupporting

confidence: 58%

Evolution of the Indian summer monsoon during the interval 32.7–11.4cal. ka BP: Evidence from the Baoxiu peat, Yunnan, southwest China

Huang

Wei

et al. 2016

Journal of Asian Earth Sciences

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“…Global climate was inferred by the δ 18 O record of the North Greenland Ice Core Project (18). Regional habitats in the Bonneville Basin were inferred from a Great Salt Lake pollen core (15), expressed as the percentage of xeric pollen taxa (Chenopodiaceae-Amaranthus+Sarcobatus+Ambrosia-type Asteraceae) (14).…”

Section: Methodsmentioning

confidence: 99%

Energy flow and functional compensation in Great Basin small mammals under natural and anthropogenic environmental change

Terry

Rowe

2015

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

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Research on the ecological impacts of environmental change has primarily focused at the species level, leaving the responses of ecosystem-level properties like energy flow poorly understood. This is especially so over millennial timescales inaccessible to direct observation. Here we examine how energy flow within a Great Basin small mammal community responded to climate-driven environmental change during the past 12,800 y, and use this baseline to evaluate responses observed during the past century. Our analyses reveal marked stability in energy flow during rapid climatic warming at the terminal Pleistocene despite dramatic turnover in the distribution of mammalian body sizes and habitat-associated functional groups. Functional group turnover was strongly correlated with climatedriven changes in regional vegetation, with climate and vegetation change preceding energetic shifts in the small mammal community. In contrast, the past century has witnessed a substantial reduction in energy flow caused by an increase in energetic dominance of smallbodied species with an affinity for closed grass habitats. This suggests that modern changes in land cover caused by anthropogenic activities-particularly the spread of nonnative annual grasslandshas led to a breakdown in the compensatory dynamics of energy flow. Human activities are thus modifying the small mammal community in ways that differ from climate-driven expectations, resulting in an energetically novel ecosystem. Our study illustrates the need to integrate across ecological and temporal scales to provide robust insights for long-term conservation and management.paleoecology | Quaternary | desert rodents | body size | invasive grass T he chronic and cumulative anthropogenic impacts of the past century have spurred considerable shifts in climates and habitats over local to global scales. Efforts to understand ecological responses to these changes have largely been focused at the species level (e.g., range shifts) over annual to decadal timescales. However, climate and habitat change impact biotas across all levels of ecological organization, from individuals to entire ecosystems. Furthermore, many ecological processes unfold over timescales inaccessible to direct observation or experimentation (1). Evaluating the response of higher-level aggregate properties (e.g., energy flow) to environmental change across centennial to millennial timescales can thus provide the temporal context needed to assess whether modern systems now fall within or outside their natural range of variability.Emphasis on species-level responses to environmental change is rooted in the paradigm that populations are highly dynamic while the aggregate properties of a community remain relatively stable and are thus more robust to perturbation. Aggregate properties have been shown to reflect resource availability (2, 3), and their stability has often been attributed to compensatory dynamics among individual species or functional groups (4). However, recent work has shown that marked change in aggrega...

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“…The model underestimates the proxy indications of warming for the far northern coastal regions of Alaska (simulated: 0.5-1 • C versus data: 5.5-6.7 • C) and Siberia (simulated: 1-2 • C versus data: 7.1-14. to NGRIP and GRIP stable water isotope estimates of annual warming of 5 • C [37,38]. Some of the observed warming may be associated with reduced elevation of the central Greenland ice sheet [9,39].…”

Section: Simulated Surface Temperatures (A) Mean Annual Surface Tempementioning

confidence: 97%

How warm was the last interglacial? New model–data comparisons

Otto‐Bliesner

Rosenbloom

Stone

et al. 2013

Phil. Trans. R. Soc. A.

171

208

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A Community Climate System Model, Version 3 (CCSM3) simulation for 125 ka during the Last Interglacial (LIG) is compared to two recent proxy reconstructions to evaluate surface temperature changes from modern times. The dominant forcing change from modern, the orbital forcing, modified the incoming solar insolation at the top of the atmosphere, resulting in large positive anomalies in boreal summer. Greenhouse gas concentrations are similar to those of the pre-industrial (PI) Holocene. CCSM3 simulates an enhanced seasonal cycle over the Northern Hemisphere continents with warming most developed during boreal summer. In addition, year-round warming over the North Atlantic is associated with a seasonal memory of sea ice retreat in CCSM3, which extends the effects of positive summer insolation anomalies on the high-latitude oceans to winter months. The simulated Arctic terrestrial annual warming, though, is much less than the observational evidence, suggesting either missing feedbacks in the simulation and/or interpretation of the proxies. Over Antarctica, CCSM3 cannot reproduce the large LIG warming recorded by the Antarctic ice cores, even with simulations designed to consider observed evidence of early LIG warmth in Southern Ocean and Antarctica records and the possible disintegration of the West Antarctic Ice Sheet. Comparisons with a HadCM3 simulation indicate that sea ice is important for understanding model polar responses. Overall, the models simulate little global annual surface temperature change, while the proxy reconstructions suggest a global annual warming at LIG (as compared to the PI Holocene) of approximately 1 ° C, though with possible spatial sampling biases. The CCSM3 SRES B1 (low scenario) future projections suggest high-latitude warmth similar to that reconstructed for the LIG may be exceeded before the end of this century.

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High-resolution record of Northern Hemisphere climate extending into the last interglacial period

Cited by 2,597 publications

References 53 publications

Evolution of the Indian summer monsoon during the interval 32.7–11.4cal. ka BP: Evidence from the Baoxiu peat, Yunnan, southwest China

Evolution of the Indian summer monsoon during the interval 32.7–11.4cal. ka BP: Evidence from the Baoxiu peat, Yunnan, southwest China

Energy flow and functional compensation in Great Basin small mammals under natural and anthropogenic environmental change

How warm was the last interglacial? New model–data comparisons

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