Abstract

Past glacials can be thought of as natural experiments in which variations in boundary conditions influenced the character of climate change. However, beyond the last glacial, an integrated view of orbital- and millennial-scale changes and their relation to the record of glaciation has been lacking. Here, we present a detailed record of variations in the land-ocean system from the Portuguese margin during the penultimate glacial and place it within the framework of ice-volume changes, with particular reference to European ice-sheet dynamics. The interaction of orbital- and millennial-scale variability divides the glacial into an early part with warmer and wetter overall conditions and prominent climate oscillations, a transitional mid-part, and a late part with more subdued changes as the system entered a maximum glacial state. The most extreme event occurred in the mid-part and was associated with melting of the extensive European ice sheet and maximum discharge from the Fleuve Manche river. This led to disruption of the meridional overturning circulation, but not a major activation of the bipolar seesaw. In addition to stadial duration, magnitude of freshwater forcing, and background climate, the evidence also points to the influence of the location of freshwater discharges on the extent of interhemispheric heat transport.

INTRODUCTION

The penultimate glacial (ca. 135–185 ka) corresponds to Marine Isotope Stage (MIS) 6, the Illinoian glaciation in North America, and the late Saalian glaciation in Europe. The latter was characterized by two major ice advances: the more extensive Drenthe, followed by the Warthe (Ehlers et al., 2011). During Marine Isotope Substage 6e (sensuMargari et al., 2010) ca. 165–179 ka, boreal summer insolation reached interglacial values and was accompanied by an intensification of monsoonal systems (Wang et al., 2008), deposition of sapropel layer S6, and pluvial conditions in the Mediterranean (Bard et al., 2002), while sea level was –40 m to –60 m relative to present (Thompson and Goldstein, 2006). In terms of millennial-scale changes, low detrital carbonate content at several North Atlantic sites (e.g., McManus et al., 1999; de Abreu et al., 2003; Hemming, 2004; Channell et al., 2012) suggests that iceberg discharges through Hudson Strait (Canada) were reduced compared to other glacials. Despite the absence of typical Heinrich events, stadial conditions persisted longer during the first part of MIS6 than comparable non-Heinrich stadials in MIS3, reflecting the influence of background climate on the strength of meridional overturning circulation (MOC) (Margari et al., 2010). Regarding terrestrial changes, apart from a few exceptions (e.g., Wang et al., 2008; Roucoux et al., 2011), there is a dearth of high-resolution records spanning MIS6. Here we return to the Portuguese margin and examine land-ocean changes during MIS6 and their relation to the record of glaciation.

SETTING AND EARLIER WORK

Previous work on the Portuguese margin has highlighted its importance for tracing millennial-scale variability and undertaking land-sea comparisons. A key aspect is that the area is located sufficiently near to the continent to derive a regional pollen signal, but deep enough to generate high-quality isotopic records that are pertinent to basin-wide phenomena. During MIS3, the δ18Oplanktonic and sea-surface temperature (SST) records closely matched the Greenland δ18Oice sequence, while the δ18Obenthic curve resembled the temperature curve from Antarctica, both in its shape and phasing relative to changes in δ18Oplanktonic (Shackleton et al., 2000; Martrat et al., 2007; Skinner et al., 2007). Concerning land-sea comparisons, joint pollen and foraminiferal isotope analyses have established the immediate response of vegetation to millennial-scale variability (e.g., Sánchez Goñi et al., 2000) and a close coupling of low- and mid-latitude hydrological changes via shifts in the mean latitudinal position of the Intertropical Convergence Zone (ITCZ) (e.g., Tzedakis et al., 2009).

MATERIALS AND METHODS

Core MD01-2444 (37°33.68′N, 10°08.53′W; 2637 m water depth; 27.45 m long) was recovered from an elevated spur on the continental rise, using the CALYPSO Giant Piston corer aboard the R/V Marion Dufresne II. In the MIS6 section of MD01-2444, sediment accumulation rates are ∼10 cm/k.y. Pollen and stable isotope analyses were undertaken on the same levels every 3 cm; X-ray fluorescence (XRF) analyses were obtained every 2 mm (see Margari et al. [2010] and Hodell et al. [2013] for methods).

Here, we use the chronology of Barker et al. (2011), based on alignment of SST changes in MD01-2444 to the synthetic Greenland (GLT-syn) record (Table DR1 in the GSA Data Repository1). GLT-syn was constructed from the European Project for Ice Coring in Antarctica (EPICA) Dome C (EDC, East Antarctica) δD record, using the bipolar-seesaw model, and placed on an absolute time frame by alignment to precisely dated Chinese speleothems for the interval 0–400 ka (Barker et al., 2011). The placement of the MD01-2444 sequence on the speleothem time scale permits an independent investigation of the phase responses of proxy records relative to orbital forcing.

RESULTS AND DISCUSSION

Millennial-Scale Changes

Millennial-scale variability is pervasive and especially prominent during the first half (185–160 ka) of MIS6 (Fig. 1), with the δ18Oplanktonic and δ18Obenthic records showing the same asynchronous phasing as observed during MIS3 by Shackleton et al. (2000), suggesting changes in surface and deep-water hydrography consistent with the operation of the bipolar seesaw (Margari et al., 2010). The alkenone-based SST reconstructions contain a similar number of oscillations (Martrat et al., 2007), but the overall profile shows relatively small and short-lived SST falls from a baseline of ∼15 °C, except for a large decrease at ca. 157–154 ka. For most of MIS6 (until ca. 145 ka), variations in temperate tree pollen percentages (Fig. 1) closely mirror the δ18Oplanktonic record, suggesting the synchronous response of vegetation to North Atlantic millennial-scale variability (Margari et al., 2010). During interstadials, arboreal populations (composed primarily of deciduous Quercus) expanded, while Mediterranean vegetation communities (mainly evergreen Quercus) were present in smaller abundance. During stadials, steppe communities (Artemisia, Chenopodiaceae, and Ephedra) were the dominant vegetation type (Fig. DR1 in the Data Repository).

The structure of millennial-scale oscillations in MD01-2444 during MIS6e is similar to that seen in speleothems from France and China (Wainer et al., 2013; Wang et al., 2008), suggesting coherent hemispheric changes in climate, as already observed in MIS3. Considering the entire MIS6 interval, we note that the temperate tree pollen record matches the Greenland GLT-syn curve of Barker et al. (2011) more closely than the δ18Oplanktonic and the alkenone SST records do. This may arise from the way the three proxies each record a differently biased or convolved measure of local conditions and how these relate to the bipolar seesaw, which is the basis of the GLT-syn curve. The fact that vegetation and hydrological changes associated with millennial-scale shifts in the ITCZ (Tzedakis et al., 2009) closely track the GLT-syn record therefore suggests that these processes are more tightly linked to the bipolar seesaw.

Orbital-Scale Changes

Hodell et al. (2013) have shown that variations in sediment composition in MD01-2444 contain strong precessional power, with the ratio of biogenic (Ca) to detrital (Ti) sediments lagging precession minima by ∼7 k.y. (Fig. 2). On orbital time scales, Ca/Ti minima in this area reflect dilution of carbonate accumulation by increased clay flux, while on millennial time scales, Ca/Ti minima correspond to cold events, reflecting decreases in carbonate productivity (Hodell et al., 2013) and/or increased detrital sedimentation (Lebreiro et al., 2009). In terms of vegetation changes, while variations in temperate tree populations are dominated by millennial-scale variability, other taxon-specific responses show a clear precessional cyclicity superimposed on millennial oscillations. Most striking is the Ericaceae (heathland) curve with three major expansions coinciding with perihelion passage in winter (Fig. 2). The expansion of Ericaceae during intervals of minimum boreal summer insolation and reduced seasonality reflects reduced summer aridity and greater annual moisture availability (Margari et al., 2007; Fletcher and Sánchez Goñi, 2008), associated with the southernmost latitudinal summer position of the ITCZ. The Ericaceae percentages closely co-vary with changes in the Ca/Ti record, which may point to a causal mechanism whereby expanded vegetation cover during times of moisture availability prevented increased erosion and discharge of detrital material by the Tagus River. Alternatively, the Ca/Ti and Ericaceae signals may represent independent but synchronous responses to climate forcing.

Integration with the Record of Glaciation

Global sea-level reconstructions (Thompson and Goldstein, 2006; Elderfield et al., 2012) indicate a sea-level fall after ca. 163 ka, likely associated with a rapid advance of the Drenthe ice sheet to its maximum extent (Fig. 3). This was followed by ice-sheet melting under increasing summer insolation and a sea-level rise at ca. 157 ka. The most extreme conditions occurred at ca. 157–154 ka, characterized by coldest SSTs, minimum δ13Cbenthic values, and a collapse of moisture-requiring temperate tree and Ericaceae populations (Fig. 3). This event appears coeval with large seasonal discharges of the Fleuve Manche river (Channel River), indicated by thick laminated facies and peaks in freshwater algae in the Bay of Biscay (Eynaud et al., 2007), originating from the rapid wasting of the Drenthe ice sheet (Toucanne et al., 2009). The correlation is also supported by maximum values in the relative proportion of tetra-unsaturated alkenones (C37:4%) in MD01-2444, which could reflect the advection of cold surface water to the Portuguese margin (Martrat et al., 2007). However, this mid-MIS6 event (Fig. 1) is accompanied by only subdued asymmetric phasing in planktonic-benthic δ18O and a particularly slow warming in Antarctica, suggesting a weak impact on interhemispheric heat transport, despite its stadial duration (3 k.y.) in the North Atlantic (cf. EPICA Community Members, 2006). An analogy has been drawn with another episode of strong Fleuve Manche discharge during Heinrich Stadial (HS) 1 (ca. 17 ka) (Toucanne et al., 2009), but HS1 was characterized by Hudson Strait–derived detrital carbonate (e.g., Hemming, 2004) and was coeval with warming in Antarctica. Earlier (but less extreme) Fleuve Manche discharges at ca. 270 and ca. 340 ka (Toucanne et al., 2009) were also associated with Hudson Strait discharges (Channell et al., 2012) and warming in Antarctica (Jouzel et al., 2012). By contrast, the absence of detrital carbonate in North Atlantic sediments during the mid-MIS6 event (Channell et al., 2012) points to reduced Hudson Strait discharges. The lack of major bipolar-seesaw activity at that time could therefore be related to the origin of freshwater discharge into the North Atlantic, which may have been predominantly European.

No major interstadial warming is indicated by the pollen and planktonic δ18O records of MD01-2444 during the small summer insolation maximum at 151 ka, and this is in concert with the lack of organic deposits and absence of paleosols in northern Europe during the interval between the Drenthe and the Warthe Stadials (Ehlers et al., 2011). After ca. 150 ka, eustatic sea-level records and glacial geological evidence suggest that ice sheets expanded, with global ice volume reaching its maximum extent toward the end of MIS6, reflecting the growth of the late Illinoian ice sheet in North America (e.g., Curry et al., 2011; Syverson and Colgan, 2011). In Europe, the Warthe I and II ice advances were less extensive than the Drenthe (Ehlers et al., 2011), but that may have been compensated for by ice expansion in Russia and Siberia (e.g., Astakhov, 2004). Compared to the last glacial maximum, late MIS6 was characterized by overall larger ice sheets, supporting the view that the strongest glacials occur when the system skips a small insolation maximum, with limited ice loss, and continues its trajectory toward increasingly colder conditions (Raymo, 1997; Paillard, 2001).

EMERGING PATTERNS

Taken together, the records of changes in the land-ocean system from the Portuguese margin form a coherent framework with the evidence of ice-volume variations during MIS6. On the basis of the amplitude of millennial-scale variability, the penultimate glacial may be divided into three parts: (1) early (185–160 ka), with prominent oscillations in foraminiferal isotope and tree pollen values; (2) transitional (160–150 ka); and (3) late (150–135 ka), with subdued benthic δ18O and δ13C and Antarctic δD variations (but with excursions in surface ocean conditions, perhaps associated with Warthe ice movements), and minimum temperate tree pollen values. This is consistent with the observation that mean climate state modulates the amplitude of millennial-scale variability (e.g., McManus et al. 1999; Tzedakis, 2005; Barker et al., 2011). More specifically, the overall warmer and wetter conditions of early MIS6 associated with the strong boreal summer insolation maximum at 175 ka, combined with excess ice of –40 m to –60 m sea-level equivalent, were marked by accentuated millennial-scale variability and activation of the bipolar seesaw. By contrast, the character of changes after 150 ka is consistent with a reduction of millennial-scale variability as climate approached a more stable maximum glacial state, which culminated into one of the largest Quaternary glaciations. However, the muted bipolar-seesaw variability during the mid-MIS6 event was not related to an extreme glacial state, as relative sea level (–35 to –65 m) was within the millennial climate instability window. We suggest that in addition to North Atlantic stadial duration (EPICA Community Members, 2006), magnitude of freshwater forcing (Ganopolski and Rahmstorf, 2001), and background climate (Margari et al., 2010), the regional distribution of ice sheets and location of freshwater discharge may have also influenced interhemispheric heat transport. Such natural experiments under different boundary conditions provide a more nuanced view of freshwater forcing, MOC sensitivity, and global climate.

The study was supported by the National Environment Research Council (grant NE/C514758/1), the European Union (grant EV K2-CT-2000-00089), and the Royal Society. We thank A. Ganopolski for discussions, F. Eynaud for providing the MD03-2692 data, and the reviewers and editor for their comments.

1GSA Data Repository item 2014065, Table DR1 and Figures DR1 and DR2, is available online at www.geosociety.org/pubs/ft2014.htm, or on request from editing@geosociety.org or Documents Secretary, GSA, P.O. Box 9140, Boulder, CO 80301, USA.