The Climate of the MIS-13 Interglacial according to HadCM3

Muri, Helene; Yin, Qiuzhen; Karami, Mehdi Pasha; Barriat, Pierre-Yves

doi:10.1175/jcli-d-12-00520.1

Cited by 24 publications

(14 citation statements)

References 55 publications

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“…Future studies should include the effects of changing ice sheets and associated meltwater fluxes in shaping interglacial climates. Large Northern Hemisphere ice sheets might have played an important role for regional and global climates, especially during early Brunhes interglacials (MIS 13 and before) as suggested by, e.g., Qiuzhen Yin et al (2008) and Muri et al (2013). Model studies suggest an influence of changing land ice on the interglacial climate evolution also during late Brunhes interglacial stages, like the Holocene (Renssen et al, 2009;Marzin et al, 2013).…”

Section: Discussionmentioning

confidence: 96%

“…A recent simulation of the MIS 13 time slice at 506 ka using the CGCM Hadley Centre Coupled Model version 3 (HadCM3) (Muri et al, 2013) can be compared to our 504 ka time slice using CCSM3. Global patterns of surface temperature anomalies (relative to PI) are remarkably similar in the two different simulations with warm anomalies over all continents (except for the northern African and South Asian monsoon regions) in boreal summer and worldwide cold anomalies during boreal winter.…”

Section: Discussionmentioning

confidence: 99%

“…Braconnot et al, 2007;, earlier interglacial periods have received much less attention by climate modellers. Coupled general circulation model (CGCM) studies of earlier interglacial climates have recently been performed for Marine Isotope Stage (MIS) 11 (Milker et al, 2013;Kleinen et al, 2014) and MIS 13 (Muri et al, 2013). Using the CGCM CCSM3 (Community Climate System Model version 3), Herold et al (2012) presented a set of interglacial climate simulations comprising the interglaciations of MIS 1, 5, 9, 11, and 19.…”

Section: Introductionmentioning

confidence: 99%

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Intra-interglacial climate variability: model simulations of Marine Isotope Stages 1, 5, 11, 13, and 15

2016

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Abstract. Using the Community Climate System Model version 3 (CCSM3) including a dynamic global vegetation model, a set of 13 time slice experiments was carried out to study global climate variability between and within the Quaternary interglacials of Marine Isotope Stages (MISs) 1, 5, 11, 13, and 15. The selection of interglacial time slices was based on different aspects of inter-and intra-interglacial variability and associated astronomical forcing. The different effects of obliquity, precession, and greenhouse gas (GHG) forcing on global surface temperature and precipitation fields are illuminated. In most regions seasonal surface temperature anomalies can largely be explained by local insolation anomalies induced by the astronomical forcing. Climate feedbacks, however, may modify the surface temperature response in specific regions, most pronounced in the monsoon domains and the polar oceans. GHG forcing may also play an important role for seasonal temperature anomalies, especially at high latitudes and early Brunhes interglacials (MIS 13 and 15) when GHG concentrations were much lower than during the later interglacials. High-versus low-obliquity climates are generally characterized by strong warming over the Northern Hemisphere extratropics and slight cooling in the tropics during boreal summer. During boreal winter, a moderate cooling over large portions of the Northern Hemisphere continents and a strong warming at high southern latitudes is found. Beside the well-known role of precession, a significant role of obliquity in forcing the West African monsoon is identified. Other regional monsoon systems are less sensitive or not sensitive at all to obliquity variations during interglacials. Moreover, based on two specific time slices (394 and 615 ka), it is explicitly shown that the West African and Indian monsoon systems do not always vary in concert, challenging the concept of a global monsoon system on astronomical timescales. High obliquity can also explain relatively warm Northern Hemisphere high-latitude summer temperatures despite maximum precession around 495 ka (MIS 13). It is hypothesized that this obliquity-induced high-latitude warming may have prevented a glacial inception at that time.

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Section: Discussionmentioning

confidence: 96%

Section: Discussionmentioning

confidence: 99%

Section: Introductionmentioning

confidence: 99%

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Intra-interglacial climate variability: model simulations of Marine Isotope Stages 1, 5, 11, 13, and 15

2016

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“…Unexpectedly, they also found that a small Eurasian ice sheet reinforces additionally the EASM through a topographically induced wave train, which might explain the exceptional EASM during MIS-13. These findings have been confirmed by more complex general circulation models including an atmosphere-only model ARPEGE Muri et al, 2012) and an atmosphere-ocean coupled model HadCM3 (Muri et al, 2013). However, it is still unclear if there was any other ice sheet than Greenland in the NH during MIS-13 because some terrestrial proxies seem to indicate a relatively warm condition during this interglacial (Guo et al, 2009).…”

Section: Introductionmentioning

confidence: 63%

“…"MIS-13" insolation means the insolation at 506 ka BP. "MIS-13" SST means the simulated MIS-13 SST by Muri et al (2013) using the atmosphere-ocean coupled model HadCM3 forced by the MIS-13 insolation and greenhouse gas concentrations. "Warmer warm pool" SST is the same as "MIS-13" SST except that the SST over the IPWP is increased.…”

Section: Introductionmentioning

confidence: 99%

Relative impact of insolation and the Indo-Pacific warm pool surface temperature on the East Asia summer monsoon during the MIS-13 interglacial

et al. 2014

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Abstract. During Marine Isotope Stage (MIS)-13, an interglacial about 500 000 years ago, the East Asian summer monsoon (EASM) was suggested exceptionally strong by different proxies in China. However, MIS-13 is a weak interglacial in marine oxygen isotope records and has relatively low CO 2 and CH 4 concentrations compared to other interglacials of the last 800 000 years. In the meantime, the sea surface temperature (SST) reconstructions have shown that the warm pool was relatively warm during MIS-13. Based on climate modeling experiments, this study aims at investigating whether a warmer Indo-Pacific warm pool (IPWP) can explain the exceptionally strong EASM occurring during the relatively cool interglacial MIS-13. The relative contributions of insolation and of the IPWP SST as well as their synergism are quantified through experiments with the Hadley Centre atmosphere model, HadAM3, and using the factor separation technique. The SST of the IPWP has been increased based on geological reconstructions. Our results show that the pure impact of a strong summer insolation contributes to strengthen significantly the summer precipitation in northern China but only little in southern China. The pure impact of enhanced IPWP SST reduces, slightly, the summer precipitation in both northern and southern China. However, the synergism between insolation and enhanced IPWP SST contributes to a large increase of summer precipitation in southern China but to a slight decrease in northern China. Therefore, the ultimate role of enhanced IPWP SST is to reinforce the impact of insolation in southern China but reduce its impact in northern China. We conclude that a warmer IPWP helps to explain the strong MIS-13 EASM precipitation in southern China as recorded in proxy data, but another explanation is needed for northern China.

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Interglacials of the last 800,000 years

2016

Reviews of Geophysics

397

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Interglacials, including the present (Holocene) period, are warm, low land ice extent (high sea level), end-members of glacial cycles. Based on a sea level definition, we identify eleven interglacials in the last 800,000 years, a result that is robust to alternative definitions. Data compilations suggest that despite spatial heterogeneity, Marine Isotope Stages (MIS) 5e (last interglacial) and 11c (~400 ka ago) were globally strong (warm), while MIS 13a (~500 ka ago) was cool at many locations. A step change in strength of interglacials at 450 ka is apparent only in atmospheric CO 2 and in Antarctic and deep ocean temperature. The onset of an interglacial (glacial termination) seems to require a reducing precession parameter (increasing Northern Hemisphere summer insolation), but this condition alone is insufficient. Terminations involve rapid, nonlinear, reactions of ice volume, CO 2 , and temperature to external astronomical forcing. The precise timing of events may be modulated by millennial-scale climate change that can lead to a contrasting timing of maximum interglacial intensity in each hemisphere. A variety of temporal trends is observed, such that maxima in the main records are observed either early or late in different interglacials. The end of an interglacial (glacial inception) is a slower process involving a global sequence of changes. Interglacials have been typically 10-30 ka long. The combination of minimal reduction in northern summer insolation over the next few orbital cycles, owing to low eccentricity, and high atmospheric greenhouse gas concentrations implies that the next glacial inception is many tens of millennia in the future. Introduction-Interglacials of the Last 800 kaEarth's climate of the last 800 ka (1 ka = 1000 years) is the latest stage in a slow cooling that has been in progress for the last~50 Ma (1 Ma = 1 million years) [Zachos et al., 2008]. During this cooling, ice sheets formed on the Antarctic continent~40 Ma ago, while the first signs of Northern Hemisphere (NH) glaciation appeared much more recently. Only at the start of the Quaternary Period and the Pleistocene Epoch,~2.6 Ma ago, did alternations between cold glacial periods with ice on the NH continents, and warmer intervals with little or no NH continental ice, first appear, reflected in the appearance of ice-rafted debris Kleiven et al., 2002] and in enhanced amplitude of cyclicity in benthic oxygen isotopes in marine sediment records (Figure 1) [Lisiecki and Raymo, 2005].Somewhere between 1.2 and 0.6 Ma ago, weaker cycles with a period of~40 ka gave way to stronger (greater isotopic amplitude) cycles with a recurrence period closer to 100 ka. This change is known as the Mid-Pleistocene Transition or Revolution. Its exact date is debated, and it is likely that different aspects of climate shifted into their new mode of operation at different times [Mudelsee and Schulz, 1997;Rutherford and D'Hondt, 2000;Clark et al., 2006;Elderfield et al., 2012]. By 800 ka ago, the change in amplitude was complete in most re...

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The Climate of the MIS-13 Interglacial according to HadCM3

Cited by 24 publications

References 55 publications

Intra-interglacial climate variability: model simulations of Marine Isotope Stages 1, 5, 11, 13, and 15

Intra-interglacial climate variability: model simulations of Marine Isotope Stages 1, 5, 11, 13, and 15

Relative impact of insolation and the Indo-Pacific warm pool surface temperature on the East Asia summer monsoon during the MIS-13 interglacial

Interglacials of the last 800,000 years

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