D. Wolf et al. 
across Europe, pointing to variable effects of different D-O 
avents (Fletcher et al., 2010; Sänchez Gofi et al., 2018; see 
also Torner et al., 2019). On the other hand, Greenland stadi- 
als (GS) were generally linked with marine cold spells in the 
North Atlantic with severe effects on marine dynamics as 
well as on vegetation development, especially in SW Europe. 
In this context, Heinrich Events (HE) (Heinrich, 1988; 
Broecker, 1994) that presumably strongly altered the thermo- 
haline circulation as the main heat supplier to the NE Atlantic 
were related to the most drastic marine temperature drops dur- 
ing the last glacial period, with equally strong effects on con- 
tinental environments in Iberia (Cacho et al., 1999; Bard 
et al., 2000; Sänchez Goni et al., 2000; Moreno et al., 
2005; Roucoux et al., 2005; Salgueiro et al., 2010). As 
noted by Ganopolski and Rahmstorf (2001), marine cooling 
linked to HEs was most pronounced in the subtropical Atlan- 
tic instead of the northern Atlantic where conditions were 
already cold. At the Iberian margin, in addition to the detec- 
tion of ice-rafted debris (IRD) and strong declines of North 
Atlantic SSTs, a dramatic decrease of thermophilous flora 
over the Iberian mainland has also been related to Heinrich 
stadials (HS; stadials comprising Heinrich Events, see, e.g., 
Sänchez Gofii and Harrison, 2010) (Turon et al., 2003; Rou- 
z0ux et al., 2005). Given the close proximity to the North 
Atlantic, a strong effect of marine cold spells on terrestrial 
systems of the Iberian Peninsula should be expected, in par- 
ticular when related to HEs. But apart from Iberian marine 
records and some findings mainly from the northern Iberian 
mainland (Gonzälez-Samperiz et al., 2006; Moreno et al., 
2010; Vegas et al., 2010; Ortiz et al., 2013), terrestrial records 
providing such indications are very rare (Gonzälez-Samperiz 
et al., 2010; Moreno et al., 2012). In this context, a major 
research gap exists for the central part of Iberia, which is char- 
acterized by a strong continental climate due to isolating 
effects of the framing mountain ranges. When effects of 
3 100 200 2 400 500 km 
FR 
HEs on terrestrial systems on a global scale is considered 
‘Ganopolski and Rahmstorf, 2001; Claussen et al., 2003; 
Pausata et al., 2011; Thomas et al., 2012; Han et al., 2015; 
Xiong et al., 2018), the Iberian interior seems to be particu- 
larly suitable to examine whether relations between terrestrial 
system behavior and marine cold spells (and HEs in particu- 
lar) can be established in regions linked to certain continental- 
ity. In that regard, observations have been hampered so far by 
‘he absence of appropriate archives. 
The upper Tagus Basin (Fig. 1) is part of the Iberian South- 
ern Meseta and is characterized by vast deposits of Tertiary 
zypseous and calcareous marls that have been intensely dis- 
jected during the Quaternary (Silva et al., 2017). This erosive 
environment generally prevented the preservation of sedi- 
mentary sequences during the Pleistocene except for fluvial 
ldeposits (Panera et al., 2011; Silva et al., 2013; Wolf et al., 
2013; Wolf and Faust, 2015; Wolf and Faust, 2016; Moreno 
et al., 2019), which reveal an incomplete record of the last 
zlacial period. Continuous pollen records exist almost exclu- 
sively in higher altitudes of the Spanish Central System 
‘Sierra des Gredos and Sierra de Guadarrama) and the Iberian 
Range, and are temporally restricted to the time after moun- 
:ain glaciers retreated in the course of Marine Isotope Stage 
‚MIS) 2 (Turu et al., 2018). Glacial landforms provide valu- 
able information on glacier advances and retreats in the Span- 
ish Central System (SCS; Palacios et al., 2011, 2012; 
Dominguez-Villar et al., 2013; Carrasco et al., 2015) that cor- 
relate with main environmental changes in the high mountain 
area. However, because glacier growth strongly depends on 
2oth cold temperatures and sufficient moisture availability 
‘Dominguez- Villar et al., 2013), the glacial record is largely 
insensitive to the most arid stages of the last glacial period. 
Also, the last glacial maximum (LGM) advance has generally 
overtaken deposits of older and less intensive glacier 
advances. 
06853s sections 
* Paraiso 
\illarubia 
/uentiduena 
villamanrique 
A 
= 
4, 
..x 
O0 
WD95-2047 
USA! 
3°30' 
20 km 
A 
315 WW 
Figure 1. In the left portion of the figure, location of the study area in the center of the Iberian Peninsula indicated by red square; Eagle Cave in 
the Gredos Range indicated by black star (SCS, Dominguez-Villar et al. 2013); locations of deep ocean sediment cores MD95-2042 and 
SU81-18 indicated by black stars in the Atlantic Ocean off the Iberian margin (Sänchez Goni et al., 2008). In the right portion of the figure, 
distribution of loess deposits is indicated in orange (following the geological map by de San Jose, 1973); studied sections are marked by yellow 
triangles. (For interpretation of references to color in this figure caption, the reader is referred to the web version of this article.) 
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attpns’/Aananar cambridaoe araf/carefterms https‘ /Zidal arn/10 1017/13 20720