D. Wolf et al. 
Table 1. Overview of micromorphological pedofeatures of carbonate/gypsum redistribution and bioturbation of the Fuentiduena (Fu) and 
Paraiso (Pa) sections with indication of sediment units (SU) and palaeo surfaces (PS). Blank space = absent; (*) = very rare/very weak; * = rare/ 
weak; °° = few/average; °°° = common/strong; MD = matrix depletion; H = depletion hypocoating; DI = depletion infilling; CC/CI = calcitic 
:oating/calcitic infilling; CH = calcitic hypocoating; CH-DI = compound calcitic hypocoating and depletion infilling; GC/GI= gypsum 
coating/gypsum infilling; DH-GC = compound depletion hypocoating and gypsum coating; Bio = bioturbation. 
Sample 
no, depth cm) Palaeo Surface MD DH DI CCI/CI CH CH-DI 
SU-8 (FUI1, 105) 
SU-7 (Pal10, 190) 
SU-7 (Pa9, 210) 
SU-7 (Fu2, 195) 
SU-7 (Fu3, 210) 
SU-7 (Pa8, 200) 
SU-7 (Pa7, 215) 
SU-7 (Fu4, 240) 
SU-7 (Pa6, 440) 
SU-6 (Fu5, 290) 
SU-6 (Fu6, 310) 
SU-6 (Pa5, 460) 
SU-6 (Pa4, 495) 
SU-5 (Pa3, 570) 
SU-5 (Pa2, 610) 
SU-4 (Fu7, 380) 
SU-4 (Fu8, 410) 
SU-4 (Pal, 710) 
GC/GI DH-GC Bio 
». 
“3 
‚. 
‚eb. 
) 8 
36 
‚0 
+88 
»® 
nA 
Fuentiduefa, and A3 sections to try to obtain a record from 
each sedimentary unit where possible. 
OSL dating of two samples from SU-3 (A3 section; Fig. 4) 
yielded ages of 112.6 + 11.9 and 95.4+ 9.2 ka (see Table 2 
for details). Because of clear indications of signal saturation, 
both ages should be considered as minimum ages, thus point- 
ing to a sedimentation period older than 100 ka. Because 
SU-3 mainly consists of fluvial-reworked loams and sand lay- 
ers, indicating active river dynamics, we expect that the sub- 
sequent floodplain incision, and thus terrace formation, 
started at the earliest during middle MIS 5. OSL dating 
af SU-4 suggests an accumulation around 96.5 +7.9 and 
106.3 + 10.3 ka in the Parafso section (Fig. 6), or until 80.7 
+8.1 ka in Fuentiduefa section (Figs. 2, 3), although these 
dates should be considered as minimum ages due to signs 
of signal saturation. Soil formation in SU-4 lasted until 
about 64.1 + 6.0 to 73.0 + 6.9 ka (Fig. 3), when the accumu- 
lation of unit SU-5 began. According to OSL dating, unit 
SU-5 was deposited during the early Pleniglacial (MIS 4) 
until 59.7 + 4.7 ka. Sedimentation of SU-6 took place in a 
narrow time frame in the middle of MIS 3 around 43.0 + 
4.8 to 41.3+4.0 ka (Figs. 2, 6), where the age of 41.3 + 
4.0 ka is a minimum age estimation due to clear signs of 
dose saturation within the sample. Following the accumula- 
tion of SU-6, OSL dating points towards a prolonged inter- 
ruption of loess deposition until =32.2+2.7 ka (Fig. 3). 
ın most sections, unit SU-7 is up to or more than 2-m thick, 
and accumulated in a very short time span between 
32.2+2.7 and 28.4+2.4 ka (Figs. 2, 4). The deposition of 
SU-8 took place between 25.9+2.4 and 23.2+1.6 ka 
(Figs. 4, 6). For SU-9, a single OSL date suggests deposition 
at about 16.2 + 1.4 ka (Figs. 2, 3). 
According to stratigraphical and chronological patterns, 
the following phases of surface stability linked to an interrup- 
tion of loess deposition have been detected (ages determine 
maximum time spans, especially the onset of surface stability 
may have started later): (1) PS-1 (SU-4): between 96.5 +7.9 
and 73.0+6.9 ka; (ii) PS-2 (SU-5): between 59.7 + 4.7 and 
13.0+3.8 ka; (1i) PS-3 (SU-6): between 41.3+4.0 and 
32.2 42.7 ka; (iv) PS-4 and PS-5 (SU-7): =31 ka and between 
28.4+2.4 and 25.9 + 2.4 ka. 
Environmental magnetic measurements 
Results of magnetic measurements support previous evidence 
of somewhat stronger pedogenic processes linked to PS-1 and 
PS-2 as well as reduced or no pedogenesis linked to the over- 
lying units and palaeo surfaces. 
As seen in Fig. 12, there is a clear relationship between 
higher values of low-frequency magnetic susceptibility and 
higher values of frequency-dependent magnetic susceptibil- 
ity, which indicate typical so-called magnetic enhancement, 
implying an increase of Xır solely caused by an increase of 
zuperparamagnetic particles. This relationship is most likely 
‘he result of pedogenic processes. This finding is supported 
2y the observation that all values in the upper range of the dia- 
zram belong to units SU-3 and SU-4, comprised of relocated, 
strongly weathered soil material derived from erosion of older 
surface soils (SU-3) as well as a strong, in situ paleosol 
formed during the upper MIS 5 (PS-1). The following 
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