Chronostratigraphy in karst records from the Epipaleolithic to the Mid/Early Neolithic (c. 13.0e6.0 cal ka BP) in the Catalan Coastal Ranges of NE Iberia: environmental changes, sedimentary processes and human activity

Quaternary Science Reviews xxx (2017) 1e21 

Contents lists available at ScienceDirect 

Quaternary Science Reviews 

journal homepage: www.elsevier.com/locate/quascirev 

Chronostratigraphy in karst records from the Epipaleolithic to the 

Mid/Early Neolithic (c. 13.0e6.0 cal ka BP) in the Catalan Coastal 

Ranges of NE Iberia: environmental changes, sedimentary processes 

and human activity 

M. Merce Bergada a, * , Josep M. Cervello a , Manel Edo b , Artur Cebria a , F. Xavier Oms a , 

Pablo Martínez b , Ferran Antolín b, c , Juan Ignacio Morales a , Mireia Pedro a 

a SERP, Departament d’Historia i Arqueologia, Universitat de Barcelona, C/ Montalegre, 6-8, 08001 Barcelona, Catalonia, Spain 

b CIPAG. Col·lectiu per la Investigacio de la Prehistoria i l’Arqueologia del Garraf-Ordal, Begues, Barcelona, Catalonia, Spain 

c IPAS. Integrative Prehistory and Archaeological Science, University of Basel, Basel, Switzerland 

article 

info 

abstract 

Article history: 

Received 29 March 2017 

Received in revised form 

2 August 2017 

Accepted 18 September 2017 

Available online xxx 

Keywords: 

Younger Dryas 

Middle and Early Holocene 

Rapid climate changes 

Geoarchaeology 

Micromorphology 

Stabling areas 

Karstic cave 

NE Iberian peninsula 

Cova de Can Sadurní 

Cova de la Guineu 

The stratigraphic, sedimentary and palaeoenvironmental features reflected in cavities in the Catalan 

Coastal Ranges of NE Iberia (Can Sadurní and Guineu caves) characterize the periods of pronounced 

climatic and human complexity that occurred c. 13.0e6.0 cal ka BP. This includes the stages of the 

Younger Dryas and Mid/Early Holocene, the latter being one of the periods of so-called Rapid Climatic 

Changes (RCCs). These caves, like others in Mediterranean contexts, are the result of an old duct originating 

in the saturated zone of the karst system and open to the outside; recording a succession of 

different detrital and anthropic episodes of the Epipaleolithic, Mesolithic and Neolithic communities. 

From this study it can be seen that paleoclimatic events do not always present clear signals in the karst 

records, especially c. 12.7e7.4 cal ka BP, corresponding to the Epipaleolithic and Mesolithic. It is characterized 

by a stratigraphic discontinuity in which there are phases with predominantly detrital sedimentation 

alternating with hiatus intervals. Detrital sedimentation formed by fine material colluvium 

with gravitational movements or solifluction processes in fresh and humid conditions. It appears in the 

following chronological intervals: 12.7e12.2 cal ka BP, 11.5/11.1e10.7/10.4 cal ka BP and 8.2e8.0 cal ka BP 

(less humid). Hiatus phases are represented in the rest of the sequence up to c. 7.4 cal ka BP. From the 

sedimentary point of view these stages of hiatus are indicative of phases of stability or lack of episodes 

with seasonal contrasts; a fact that would cause interruptions to detrital deposition in the interior of the 

caves. 

In contrast, in the period c. 7.4 to 6.0 cal ka BP, attributed to the Middle and Early Neolithic, there is a 

certain stratigraphic continuity. From the sedimentary point of view it is distinguished by a variability of 

processes that responds to accumulative episodes of short duration characteristic of morphogenesis of 

the slopes in an arid Mediterranean environment, identified in our records as RCCs, (c. 7.4e7.2 cal ka BP- 

Cardial Neolithic; c. 6.8e6.3 cal ka BP-Early Postcardial Middle Neolithic and c. 6.2e5.7 cal ka BP- Late 

Postcardial Middle Neolithic) alternating with episodes of stability, more humid and coinciding with a 

better sedimentary record of the pastoral activity in the cavities during Epicardial and Late Cardial 

Neolithic (c. 7.1e6.7 cal ka BP) and Postcardial Middle Neolithic (c. 6.6e5.9 cal ka BP). It is during this 

period that Holocene climate variability has better resolution in caves in the Catalan Coastal Ranges of NE 

Iberia. 

© 2017 Elsevier Ltd. All rights reserved. 

* Corresponding author. 

E-mail addresses: bergada@ub.edu (M.M. Bergada), jmcervello@gmail.com (J.M. Cervello), cipagmedo@gmail.com (M. Edo), arturcebria@gmail.com (A. Cebria), 

xavieroms@gmail.com (F.X. Oms), pablomartrod@gmail.com (P. Martínez), ferran.antolin@unibas.ch (F. Antolín), jignacio.morales@gmail.com (J.I. Morales), mireiapedro@ 

gmail.com (M. Pedro). 

https://doi.org/10.1016/j.quascirev.2017.09.008 

0277-3791/© 2017 Elsevier Ltd. All rights reserved. 

Please cite this article in press as: Bergada, M.M., et al., Chronostratigraphy in karst records from the Epipaleolithic to the Mid/Early Neolithic (c. 

13.0e6.0 cal ka BP) in the Catalan Coastal Ranges of NE Iberia: environmental changes, sedimentary processes and human activity, Quaternary 

Science Reviews (2017), https://doi.org/10.1016/j.quascirev.2017.09.008

2 

M.M. Bergada et al. / Quaternary Science Reviews xxx (2017) 1e21 

1. Introduction 

In this paper we characterize the stratigraphic, sedimentary and 

palaeoenvironmental features that are reflected in karst contexts in 

the Catalan Coastal Ranges of NE Iberia, from one of the periods 

with the greatest climatic complexity located between c. 

13.0e6.0 cal. Ka BP and of great importance for human occupations. 

These are the stages of the Younger Dryas (YD), Early Holocene and 

Middle Holocene (EH and MH), with the so-called period of Rapid 

Climatic Changes (RCCs) developed in the latter. 

The data available to date on the chronostratigraphic and 

palaeoenvironmental aspects of the Iberian Peninsula, and especially 

its Mediterranean basin, have been obtained through information 

from different proxies and reflect a high degree of 

variability. The YD has been widely detected, with internal variations 

and some regional diachronism (Cacho et al., 2010). Studies of 

marine and pollen records mainly indicate conditions of relative 

aridity and also of cold (Burjachs et al., 2016; Cacho et al., 2001; 

García-Ruiz et al., 2016; Gonzalez-Samperiz et al., 2006). Recently, 

high resolution analyzes of new speleothem records in the north of 

the peninsula have documented a double stage for the YD with an 

earlier arid phase followed by a relatively wetter period (García- 

Ruiz et al., 2016). 

From the cultural point of view, the regional sequence of this 

phase corresponds to the development of the last phases of the 

Magdalenian called Epimagdalenian or Epipaleolithic (Aura et al., 

2011). This phase is characterized by a decrease in the bone industry 

and a general predominance of backed point lithic projectiles, 

although geometric elements start to appear in some 

sequences such as Cova del Parco in the north-east peninsular 

(García-Argüelles et al., 2013; Petit et al., 2009). 

With regard to the Holocene, the climate change pattern of the 

Mediterranean region, with strong spatial and temporal variability, 

appears to be linked mainly to the availability of water from the 

hydrological system (Davis et al., 2003; Ferrer, 2015). 

Marine records indicate, sea surface temperature maximums in 

this phase of the Early Holocene (10.0e9.0 ka BP) (Cacho et al., 

2001; Martrat et al., 2007). It should also be added that 

numerous studies suggest that climatic conditions at the beginning 

of the Holocene were significantly more humid than during the 

Late Holocene. However, this optimum seems not to have been 

synchronous throughout the Iberian Peninsula. In the northern 

half, the wettest period occurred before 8.0 ka BP (Frigola et al., 

2007; Gonzalez-Samperiz et al., 2006; Morellon et al., 2009) 

whereas in the east and south of the Mediterranean area, the 

conditions were arid and dry (Cacho et al., 2001; Carrion et al., 

2010; Jalut et al., 2009). In this zone the maximum humidity 

occurred at about 8.0 ka cal BP (Carrion et al., 2010; Ferrer, 2015). 

From the cultural point of view, the Early Holocene is manifested 

by a complex episode in technological terms: the Sauveterrian 

style Epipaleolithic with triangles and segments (García- 

Argüelles et al., 2013); the appearance of stage called Early Mesolithic, 

which is a break with the previous tradition of industry of 

notches and denticulates (Aura et al., 2011); and finally, the Late 

Mesolithic with geometric microliths (mainly trapezes with abrupt 

retouch) of Tardenosian tradition (Burjachs et al., 2016). 

The oscillation at the beginning of the Middle Holocene that has 

attracted the most interest is the so-called event of 8.2, referring to 

its age (8.2 Ka BP) (Alley et al., 1997). The impact, duration and 

characteristics of this event have very different geographical expressions 

(Rohling and P€alike, 2005). In the context of Iberia, this 

event does not always present a clear signal, and in most of the 

continental pollen sequences it is not evident (Cacho et al., 2010). 

However, there are some examples in different sequences that 

show an increase in the aridity associated with this event, as in 

Laguna Medina in the south (Reed et al., 2001), in the playa Lake 

Salines (Burjachs et al., 2016) in the southeast or in the Estanya lake 

(Morellon et al., 2009) in the northeast. In the highest areas of the 

Pyrenees it is manifested as an arid and also cold event (Gonzalez- 

Samperiz et al., 2006). 

This c. 8.2 ka BP event is most clearly identified in marine records 

(Cacho et al., 2010). The reconstructions of sea-surface temperatures 

in Alboran and around the Balearic Islands indicate a 

cooling of about 2 -3 C(Cacho et al., 2001; Frigola et al., 2007). It 

should be noted that despite the relative scarcity of records clearly 

showing the impact of the 8.2, there is some archaeological evidence 

indicating a change in the distribution of prehistoric settlements 

or a depopulation coinciding with the ending of the 

Mesolithic (Berger and Guilaine, 2009; Cortes Sanchez et al., 2012; 

Fernandez and Jochim, 2010; Gonzalez-Samperiz et al., 2009; 

Morales and Oms, 2012). 

The Middle Holocene is characterized by the RCCs documented 

in the Northern Hemisphere (Alley et al., 1997; Berger et al., 2016; 

Combourieu-Nebout et al., 2013; Mayewski et al., 2004) and has 

been linked to the North Atlantic Bond events (Bond et al., 1997, 

2001). These episodes have presented controversy with the “thermal 

maximum” also designated within the Atlantic period. 

Both the palynological studies (Jalut et al., 2000; Perez-Obiol 

et al., 2011) and the limnological ones (Valero-Garces and 

Moreno, 2011) have shown a tendency towards aridity in the 

Mediterranean Iberia. Different authors confirm the millennial 

variability from the MH reflecting the sensitivity to changes in the 

system (Fletcher and Zielhofer, 2013; Jalut et al., 2000). 

From the point of view of population, it is a transcendental stage 

since it includes the early stages of production (Cardial Neolithic, 

Epicardial Neolithic and Postcardial Middle Neolithic) in the Mediterranean 

area dated c. 7.5 to 6.0 ka BP. 

In this paper we analyse in detail how these palaeoenvironmental 

variations are reflected in the studied karst contexts. 

The records we present are the Cova de Can Sadurní and Cova 

de la Guineu, located in the Catalan Coastal Ranges of NE Iberia 

(Fig. 1). They are cavities that, like others in Mediterranean contexts, 

are the result of an old duct that originated in the saturated 

zone of the karstic system and open to the outside, demonstrating 

the succession of such episodes in detail. It is also intended to 

reflect the interaction of human activity in the environment in 

order to contribute in a global way to the chronostratigraphic discussion 

of this period in the Mediterranean context of the NE of 

Iberia. 

2. Geological and archaeological background 

2.1. The geological and geomorphological setting 

The two cavities that are the object of our study are located in 

the structural unit of the Catalan Coastal Range in the NE of Iberia. It 

is characterized by a series of aligned reliefs and NE-SW depressions 

with an average width of 30 km subparallel to the coast 

between the Ebro Basin and the Valencia Trough, which is its 

emergent north-western margin. The present relief corresponds to 

the superposition of the Paleogene compressive structures that 

were involved in the formation of an intraplate mountain range up 

to the Upper Oligocene, and the Neogene extension that generated 

a system of half-grabens and raised and tilted horsts from inverse 

movement along the Barcelona, Valles - Penedes and the Camp 

fault. This isostatically raised the horsts of Garraf, among the halfgrabens 

of Barcelona (submerged at the coast) and that of the 

Valles-Penedes and the Prelitoral chain, between Valles-Penedes 

half-graben and the Ebro Basin (Bartrina et al., 1992). 

The rejuvenation of the relief in the structural highs with a 




M.M. Bergada et al. / Quaternary Science Reviews xxx (2017) 1e21 3 

Fig. 1. Location of Cova de Can Sadurní, Cova de la Guineu and the sites mentioned in the text. Numbers correspond to: 1. Arba de Biel; 2. Cueva del Seso; 3. Balma Margineda; 4. 

Font del Ros; 5. Cova del Parco; 6. Balma del Gai; 7. Molí del Salt; 8. Abric del Filador; 9. Abric de la Cativera; 10. Cova del Vidre; 11. Cueva de los Molinos; 12. Cova d'en Pardo; 13. 

Tossal de la Roca; 14. Abric de la Falguera. 

highly fractured Mesozoic limestone coverage generated karst 

systems, especially in the Garraf massif, which continued to rise 

until the Middle Miocene, about 15 Ma ago. The later evolution of 

this karst has been affected by variations in Mediterranean sea 

level, the Messinian crisis (7 Ma ago), the temperate tropical to 

subtropical paleoclimates that dominated the sector until the 

implementation of the Mediterranean seasonal regime 2.7 Ma ago 

and climatic fluctuations of the Pleistocene. 

The cave of Can Sadurní is located in the Garraf massif in Begues 

(Baix Llobregat, Barcelona) at 421 m ASL and UTM 409085E and 

4578770N. It is located to the south of the metropolitan area of 

Barcelona, between the valley and the delta of the river Llobregat, 

the depression of the Penedes and the Mediterranean coast. Garraf 

forms an extensive mountainous coastline that rises 600 m above 

the beaches of Castelldefels and Sitges. 

The geological map of the surroundings of Can Sadurní and 

Begues shows the complexity of Garraf geology (Fig. 2a and b). At 

the base of the massif, towards the valley and the delta of the 

Llobregat is a Palaeozoic metamorphic basement on which a thick 

Mesozoic coverage is located, intensely fractured by the alpine 

tectonics. The landscape that characterizes the massif is formed by 

the Jurassic and Cretaceous dolomites and limestones in which a 

karst with all surface modelling attributes and hundreds of subterranean 

cavities have been developed (Bergada et al., in press). 

The Garraf massif is formed by highlands furrowed by valleys 

and canyons, with poljes, clint and doline fields as well as chasms 

and caves in the upper parts. Water infiltration drains underground 

through the entire massif to the coastline. 

Fig. 2. Geological location. 

a. General map of the geological units of the caves studied. 

b. Detailed map of Cova de Can Sadurní. 

c. Detailed map of Cova de la Guineu. 

(Source: Geological Cartography of the Institut Cartografic i Geologic de Catalunya e ICGC e Generalitat de Catalunya). 




4 


The cave of Guineu located in Font-Rubí (Alt Penedes, Barcelona) 

at about 734 m ASL and UTM 380921E 4588723N. It is situated on 

the southern slope of the Prelitoral Mountain Range in the Sierra de 

Font-Rubí which is part of the horst of the Gaia and El Camp massif 

and the Montmell reliefs. 

The lithology of the site (Fig. 2a and c) consists of materials from 

the Triassic, mainly from the Upper Muschelkalk, consisting of 

micritic limestones at the base and fine-grained dolomites at the 

top (Amigo, 1983; Bergada, 1998). The total thickness in this sector 

is 50 m. The structure of this zone is conditioned almost exclusively 

by the fracturing, in which the faults with NW-SE orientation 

dominate. 

The karst system that developed in this dolomitic and limestone 

mass presents a state of important evolution. There are numerous 

endokarstic forms that have been favoured by the tectonics of the 

area. 

Morphologically the two cavities present the characteristics of 

an old duct (Fig. 3a, b, 4a and 4b) originating in the saturated zone 

of a long and complex karst system. 

Its evolution, similar to other cavities in the sector, is marked by 

a series of stages: 

a. Formation of the cavity from discontinuities in the limestone 

rock, stratification planes and subvertical tectonic 

microstructures. 

b. Dissolution in walls and roof as a result of flooded cavity regime. 

c. General lowering of the karst base level and new position of the 

cavity in the unsaturated infiltration zone of the karstic system. 

The non-soluble fraction is located in the interior of the ducts 

and consists of silt and hardened red clays derived from the 

superficial karstification processes, especially active under the 

soil cover. It is located in the eastern part of the cave room in Can 

Sadurní. 

d. Precipitation of speleothems in the cavity in the form of flowstone 

and stalagmites. 

e. Opening or enlarging of the cavities to the exterior, formation of 

clastic collapses, cones with blocks that prograde towards the 

interior and introduction of finer materials. The blocks form a 

steep ramp towards the interior of the cave, forming an 

important sedimentary deposit that includes mostly the sequences 

that are the object of this paper. 

In conclusion, the karst development in these sectors is polyphasic 

and the studied detrital deposits are recent within the 

evolution of the cavities. The analyzed sequences are essentially a 

Holocenic product of contributions from the exterior, although in 

Guineu and possibly in Can Sadurní they are situated on Pleistocene 

deposits. 

2.2. Archaeological sequences and radiocarbon dates 

The two sites that are the object of study comprise prolonged 

time sequences that have been comprehensively radiocarbon 

dated. 

2.2.1. Cova de Can Sadurní 

The site of Cova de Can Sadurní has an archaeological sequence 

that begins, according to the current state of knowledge, in the 

Epipaleolithic and reaches the Late Roman Empire. It highlights the 

Neolithic especially its early phase (Edo et al., 2011, in press a; in 

press b). 

The cavity has been known archaeologically since 1945 but no 

systematic excavations were carried out until 1978, which then 

continued uninterruptedly until present. It has two areas: in the 

exterior of the cavity under the denomination “outside terrace” of 

about 400 m 2 where occupations of the Postcardial Middle 

Neolithic were located next to silos; and inside the cave, which is 

the main sector and the object of our study in this paper. 

The excavated surface of the cave is 51 m 2 of which 4 m 2 

correspond to a sondage that began in 1997 (Fig. 3c) with the aim of 

establishing the stratigraphic sequence of the site (Edo et al., 2011). 

The data available from the Epipaleolithic to the Early Postcardial 

Middle Neolithic were obtained only from the sondage. 

So far, there have been 14 sedimentary (Bergada et al., in press) 

and 21 archaeological levels that frame the chronocultural evolution 

of the deposit from the archaeological materials; as well as the 

radiocarbon dates (Table 1) and numismatic record for the historical 

stages (Blasco et al., 2005a, 2005b; Edo et al., 2011; Edo et al. in 

press b). 

The record begins in the Epipaleolithic (CS. XIV and archaeological 

level 21) dated c.12.7e10.4 cal ka BP. This is followed by 

CS.XIII (archaeological levels 20 and 19), which is attributed to the 

Mesolithic period of denticulates and notches (Fullola et al., 2011) 

and dated 8.2e8.0 cal ka BP. After that, a beginning of pastoral 

activities and a sepulchral use appear in CS.XII (archaeological level 

18) corresponding to the Cardial Early Neolithic, most likely between 

7.4 and 7.2 cal ka BP. The subsequent Late Cardial Neolithic 

CS XI (levels 17 and 16) dated 7.2e6.6 cal ka BP and CS.X dated 

6.9e6.7 cal ka BP are characterized by the Epicardial Neolithic 

(levels 15e13), both with a pastoral use of space. CS.IX (level 11b) 

follows, eroding the underlying level in some sectors. This episode 

is dated 6.8e6.3 cal ka BP and corresponds to the Early Postcardial 

Middle Neolithic. 

The sequence continues, within the same cultural stage, with 

CS.VIII (level 11) dated 6.5e5.9 cal ka BP. The cavity was also used 

for a pastoral and funerary use. A sepulchral use of the cavity is 

mainly detected in the Late Postcardial Middle Neolithic (CS, VII-VI 

and levels 10b and 10) dated c. 6.2e5.7 cal ka BP. 

2.2.2. Cova de la Guineu 

This site also includes a wide cultural sequence (Bergada, 1998; 

Equip Guineu, 1995); although the greatest potential is offered by 

the record corresponding to the Upper Pleistocene, located in a 

sondage inside the cave. 

The cavity was discovered in 1961 but the archaeological excavations 

did not start until 1983. After a five-year break, they were 

activated again and continue to the present day. 

Unlike Can Sadurní, the aim of our study focuses mainly on the 

outside sector (Fig. 4c), with an excavated area of 21 m 2 in which 

occupations of a Late Cardial Neolithic have been located as well as 

the medieval and modern epochs. The sector of the cavity is represented, 

at the moment, from the Epipaleolithic to the Late 

Neolithic e Chalcolithic with an excavation area of 11 m 2 ; where 

the Epipaleolithic and Upper Pleistocene sequence was located in a 

sondage. So far, 12 sedimentary levels have been located (Bergada, 

1998). 

The studied sequence begins with G. IIIa dated c.12.7e11.1 cal ka 

BP (Table 2) and situated in the Mediterranean Epipaleolithic 

(Bartrolí et al., 1992). After that, there is a Late Cardial Neolithic 

referenced by G. Ie (outside sector) dated 7.1e6.9 cal ka BP (Oms 

et al., 2016); then G.II, Postcardial Middle Neolithic by the pottery, 

located with some materials from the Cardial Neolithic; followed 

by G. IIb, which corresponds to a stabling area (Bergada et al., 

2005a) dating from 6.4 to 5.9 cal ka BP; and finally, G. Id, which in 

some sectors towards the cavity has some contact with the levels of 

upper pen of the sector of the cave. Culturally, it corresponds to an 

intermediate and final moment of the Molinot Postcardial Neolithic 

and is dated 6.3e5.9 cal ka BP. 





Fig. 3. Cova de Can Sadurní (Begues, Barcelona). a. Cave entrance (arrow). b. Overview through the cavity and sedimentary deposit, with an arrow to the sondage. c. Plan of the 

cavity. d. J e 8 Sondage profile. CS.XII e CS.VI. e. J/8e7 Grid-square. CS. XIV e CS. VIII. f. Stratigraphic profile represented. 




6 


Fig. 4. Cova de la Guineu (Font-Rubí, Barcelona). a. Cave entrance (arrow). b. Overview through the cavity and sedimentary deposit, with an arrow to the sondage. c. Plan of the 

cavity. d. Stratigraphic profiles represented. 

3. Methods 

The methodology we used consisted mainly of stratigraphicsedimentary 

field descriptions and application of micromorphology 

to the levels that include the sequence of the sites. To carry 

out this study we focused mainly on the following profiles: in Can 

Sadurní profiles F-8, J-8; J-F/7, J-F/9 and G-4; and in Guineu profiles 

E5 and C5 in the interior of the cavity and E-9, F9-F7 in the exterior 

of the cavity (Fig. 3c, d, 3e, 3f, 4c and 4d). 

The protocol followed for extracting samples, a total of 21, 

consisted of placing the sediments into boxes lined with plaster, 

enabling us to obtain blocks without altering the structure and the 

position of the sedimentary filling (Bergada, 1998; Bergada et al., in 

press). The blocks were air-dried and then oven dried at 40 C for 

48 h to avoid recrystallization. They were impregnated with a 

polystyrene resin. They were cut into strips a few centimeters thick 





Table 1 

Cova de Can Sadurní. Radiocarbon dates. 

Can Sadurní 

Sedimentary layers 

Can Sadurní 

Archaeological layers 

Sample Laboratory BP Dating CalBP p(95%) CalBC Period 

CS.VI 10 Seed OxA-15490 5279 ± 31 BP 6220e5940 4270e3990 Late Postcardial Middle Neolithic 

CS.VII 10b Charcoal UBAR-1281 5075 ± 40 BP 5950e5710 4000e3760 Late Postcardial Middle Neolithic 

CS.VII 10b Human bone Beta-210652 5340 ± 40 BP 6280e5960 4330e4010 Late Postcardial Middle Neolithic 

CS.VII 10b Human bone UBAR-1282 5260 ± 40BP 6230e5870 4280e3920 Late Postcardial Middle Neolithic 

CS.VIII 11 Bone Beta- 332263 5240 ± 40 BP 6190e5870 4240e3920 Postcardial Middle Neolithic 

CS.VIII 11 Human bone Beta 197134 5290 ± 40 BP 6220e5940 4270e3990 Postcardial Middle Neolithic 

CS.VIII 11 Charcoal I-17918 5350 ± 150 BP 6440e5800 4490e3850 Postcardial Middle Neolithic 

CS.VIII 11 Charcoal UBAR-1193 5370 ± 45 BP 6340e5980 4390e4030 Postcardial Middle Neolithic 

CS.VIII 11 Human bone Beta-363819 5460 ± 40 BP 6340e6180 4390e4230 Postcardial Middle Neolithic 

CS.VIII 11 Charcoal I-13314 5470 ± 110 BP 6500e5980 4550e4030 Postcardial Middle Neolithic 

CS.VIII 11 Charcoal UBAR 766 5470 ± 140 BP 6560e5920 4610e3970 Postcardial Middle Neolithic 

CS.VIII 11 Human bone OxA-29640 5487 ± 33 BP 6360e6200 4410e4250 Postcardial Middle Neolithic 

CS.VIII 11 Bone Beta-363818 5540 ± 40 BP 6430e6270 4480e4320 Postcardial Middle Neolithic 


CS.VIII 11 Human bone OxA-29641 5568 ± 34 BP 6440e6280 4490e4330 Postcardial Middle Neolithic 

CS.VIII 11 Bone Beta-238657 5570 ± 40 BP 6440e6280 4490e4330 Postcardial Middle Neolithic 


CS.VIII 11 Seed Beta-445238 5670 ± 30 BP 6510e6390 4560e4440 Postcardial Middle Neolithic 

CS.VIII 11 Seed Beta- 445239 5680 ± 30 BP 6520e6400 4570e4450 Postcardial Middle Neolithic 

CS.VIII 11 Charcoal Beta-394625 5730 ± 30 BP 6640e6440 4690e4490 Postcardial Middle Neolithic 

CS.IX 11b Seed UBAR-846 5635 ± 45 BP 6530e6290 4580e4340 Early Postcardial Middle Neolithic 

CS.IX 11b Charcoal I-11789 5700 ± 110 BP 6750e6270 4800e4320 Early Postcardial Middle Neolithic 

CS.IX 11b Charcoal Beta-210653 5790 ± 40 BP 6690e6490 4740e4540 Early Postcardial Middle Neolithic 

CS.IX 11b Charcoal I-11787 5800 ± 160 BP 6990e6270 5040e4320 Early Postcardial Middle Neolithic 

CS.X 12 Organic material CNA -3172.1.2 5790 ± 36 BP 6690e6490 4740e4540 Early Postcardial Middle Neolithic 

CS.X 14 Charcoal Beta-179900 5980 ± 40 BP 6940e6700 4990e4750 Epicardial Neolithic 

CS.XI 17 Charcoal Beta-127898 6050 ± 110 BP 7240e6640 5290e4690 Late Cardial Neolithic 

CS.XII 18 Seed OxA-15491 6375 ± 34 BP 7430e7230 5480e5280 Cardial Neolithic 


CS.XII 18 Seed UBAR 760 6405 ± 50 BP 7470e7230 5510e5310 Cardial Neolithic 


CS.XIII 20 Charcoal Beta-230733 7320 ± 50 BP 8240e8000 6290e6050 Mesolithic 

CS.XIV 21 Charcoal Beta-179899 9360 ± 40 BP 10710-10470 8760e8520 Epipaleolithic 

CS.XIV 21 Bone Beta-230734 10540 ± 60 BP 12770-12290 10820-10340 Epipaleolithic 

Table 2 

Cova de la Guineu. Radiocarbon dates. 

Guineu Sedimentary layers Sample Laboratory BP Dating CalBP p(95%) CalBC Period 

G.Id Molar Ovis aries OxA-29605 5274 ± 32 BP 6230e5910 4280e3960 Late Postcardial Middle Neolithic 

G.Id Molar Ovis/Capra Beta-406997 5430 ± 30 BP 6310e6190 4360e4240 Late Postcardial Middle Neolithic 

G.Ie Charcoal Laurus nobilis Beta-406998 6140 ± 30 BP 7200e6920 5250e4970 Late Cardial Neolithic 

G.IIb Charcoals Gif-11037 5480 ± 60 BP 6410e6170 4460e4220 Postcardial Middle Neolithic 

G.IIb Charcoal (LC) GifA-99112 5330 ± 70 BP 6300e5940 4350e3990 Postcardial Middle Neolithic 



G.IIIa Charcoals Gif-8439 9850 ± 80 BP 11520-11120 9570e9170 Epipaleolithic 

G.IIIa Charcoal (H) Beta-378799 10590 ± 40 BP 12720-12560 10770-10610 Epipaleolithic 

LC. Layer cake. 

H. Hearth. 

and finally thin sections were made, a total of 2 for each block of 

13.5 5.5 cm and 20 mm thick according to the protocol of 

Benyarku and Stoops (2005). 

Thin sections were observed under a polarizing stereomicroscope 

and a petrographic microscope at magnifications between 

25 and 400 with plane polarized light (PPL), crossed polarized 

light (XPL) and with oblique incident light (OIL). Descriptions followed 

the criteria used by Bullock et al. (1985) and Stoops (2003). 

The dates of the two sites, altogether 43, were calibrated using 

CalPal software (Weninger et al., 2007) and compared with the d 18 O 

variation curves of the NGRIP and GRIP according to GICC05 Age 

Model (Lowe et al., 2008) (see Fig. 8); as well as the dating of the 

deposits treated in Fig. 9. 

4. Results and interpretation 

The stratigraphic, sedimentary and micromorphological data of 

the studied records are detailed in Tables 3e6. 

4.1. Pedosedimentary processes located between c. 13e6.0 cal ka BP 

The sedimentary processes of detrital origin that form the filling 

of Can Sadurní and Guineu are: solifluction, gravitational and colluvium 

and diffuse runoff. 

4.1.1. Solifluction processes 

These are found in the Epipaleolithic (CS. XIV 12.7e12.2 and 

10.7e10.4 cal ka BP) and Mesolithic sequences (CS. XIII 8.2e8.0 cal 




8 


Table 3 

Synthesis of the stratigraphic and sedimentary field description of the Cova de Can Sadurní. 

Can Sadurní 

Sedimentary 

layers 

Can Sadurní 

Archaeological 

layers 

Thickness 

(cm) 

Colour Course fraction Fine fraction Boundaries Organic and inorganic 

components 

Cultural context 

CS.VI 10 13 5YR 4/2 Some stones and blocks 

scattered. 

Sandy silts with 

clays 

Difusse 

CS.VII 10b 20e25 7.5YR 5/2 Subangular stones of 1e6 cm Clayey silts with Erosive 

and angular blocks of medium sands 

contact 

size. 

CS.VIII 11 72 5YR 6/1 Scattered stones. Clayey silts with 

sands 

CS.IX 11b 17e20 5YR 5/2 Subangular blocks and stones. Clayey silts with 

some sandy 

fraction 

CS.X 

CS.X.1 12 3e6 10YR 3/2 

10YR 6/2 

Late Postcardial 

Middle Neolithic 

Late Postcardial 


Sharp Lots of charcoal remains Postcardial 


Erosive 

Early Postcardial 

contact 


Some sand Sharp Carbonated ash accumulation 

with charcoals and organic 

remains 

Early Postcardial 


CS.X.2 13 5 10YR 5/2 Clayey silts Sharp Many charcoals Epicardial 

Neolithic 

CS.X.3 14 3e6 10YR 6/2 Subangular and subrounded 

stones and gravels. 

Clayey silts Difusse Epicardial 


CS.X.4 15 5e10 10YR 4/2 Clayey silts with 


Sharp Presence of charcoals Epicardial 


CS.XI 16, 17 19 (16) 10YR 6/ Some stones and blocks Silty sands Sharp Late Cardial 

8 (17) 5YR scattered. 


4/3 

CS.XII 18 30e35 5YR 4/2 Subangular blocks and stones. Clayey silts with 


Sharp Abundant bone and charcoal 

remains 

Cardial Neolithic 

CS.XIII 19, 20 9e35 5YR 4/4 Subrounded and subangular 

gravels and stones (1e2 cm). 

CS.XIV 21 53 7.5YR 5/4 Subangular stones and blocks 

scattered. 

*The lithology is micritic limestone. 

Clayey silts with 


Clayey silts with 


Sharp Lots of charcoal remains Mesolithic of 

Notches and 

Denticulates 

Sharp Charcoal and bone remains Epipaleolithic 

Table 4 

Synthesis of the stratigraphic and sedimentary field description of the Cova de la Guineu. 

Guineu 

Sedimentary 

layers 

Thickness (cm) Colour Course fraction Fine fraction Boundaries Organic and inorganic components Cultural context 

G.Id 54 7.5YR 3/2 Subrounded blocks 

and stones. 

Clayey silt 

with sands 

Sharp Puntuaction organic matter Late Postcardial 


G.Ie 

8 (seen at the 7.5YR 4/4 Subrounded and Sandy clays Difusse Late Cardial Neolithic 

moment) 

subangular blocks. 

G.IIb 25e35 5YR 8/1 5YR 4/2 Some stones and Some sands Sharp Carbonated ash accumulation with Postcardial Middle 

5YR 4/4 gravels. 

charcoals and organic remains 


G.II 75 7.5YR 3/2 Subrounded blocks 

and stones. 

Sandy silt 

with clays 

Erosive 

contact 

Abundant charcoals 

Postcardial Middle 


G.IIIa 34 7.5YR 6/4 Subangular stones. Sandy silt 

with clays 

Difusse 

Epipaleolithic 

*The lithology is dolomitic limestone. 

ka BP) from Can Sadurní. From the stratigraphic and sedimentary 

point of view they are characterized mainly by an orientation of the 

stones parallel to the slope of the deposit due to mass movement 

(Bertran and Texier, 1999). There are episodes, mainly in CS. XIII, 

with stones alongside others in which clayey silt dominates. According 

to Bertran and Coutard (2004) these are characteristic of 

the flow front that buries materials from the upper levels that 

would have been the first to move. 

From the micromorphological point of view, distinctive features 

are observed in this type of processes: 

CS.XIV is characterized by the vesicular microstructure (Fig. 5a) 

that is common in contexts with clayey silt matrix and under 

conditions of water saturation in which the air of the soil is 

retained. This liquefaction can be caused, in this case, by the thaw 

that creates a mass movement (Bertran and Coutard, 2004; Van 

Vliet-Lano€e, 2010). 

As pedofeatures, we highlight the traces of clay illuviation, 

located mainly in the sides of voids of the matrix (Fig. 5b). This 

process is common in this type of deposit and would indicate the 

presence of water and non-flocculating conditions (decarbonated 

soils), characteristic of humid and percolating contexts. As a 

consequence, dissolution processes are observed in the limestone 

material, in ash waste and in the bones (Fig. 5c), with the formation 

of phosphate (apatite) hypocoatings in the detrital material that is 

typical of areas rich in phosphate; in this case originating from the 

bones and reacting with the limestone material to produce a 





Table 5 

Synthesis of the micromorphological analysis description of the Cova de Can Sadurní. 

Can Sadurní 

Sedimentary 

layers 

Can Sadurní 


layers 

Microfacies Micromorphology Pedosedimentary and 

anthropic processes 

Cultural 

context 

CS. VI 10 Sandy silts with stones and 

reworked herbivore 

excremental aggregates 

Microstructure: granular. 25% porosity. Groundmass: c/f Colluvium 

50 mm 1/3. Relative distribution: porphyric. Charcoals (***), 

bones (****) and herbivore excrement fragments (**) 

inclined and vertical arrangement. Calcitic crystallitic b- 

fabric. Pedofeatures: granular bioaggregates (þþ), Ca 

hypocoatings and P-Ca hypocoatings (þ), Fe (hydr)oxides 

orthic nodules (þþþ) and clay coatings (þ). 

Late 

Postcardial 

Middle 


CS. VIII 11 Layers of phytoliths and 

organo-phosphated herbivore 

excrements 

in situ 

Thickness: 7 cm. Microstructure: subangular blocky, platy 

and massive. 25% porosity. Groundmass: c/f 50 mm 1/2. Silty 

clays with fine sands. Relative distribution: porphyric. 

Charcoals (***), articulated/disarticulated Si phytoliths 

aggregates (****), faecal spherulites (*), bones (*), bird 

eggshells (*) and herbivore excrements (cattle *** and 

ovicaprine **). Calcitic crystallitic and undifferentiated b- 

fabric. Amorphous yellow (*). Pedofeatures: granular 

bioaggregates (þþ), Ca coatings (þ) and Fe (hydr)oxides 

nodules (þþ). 

Stabling areas without 

combustion with diffuse runoff 

and trampling 

Postcardial 



CS. VIII 11 Sandy silts with phosphatized 

herbivore excremental 

aggregates 

Microstructure: granular/platy. 10e20% porosity. 

Diffusse runoff and detrital 

Groundmass: c/f 50 mm 1/3. Relative distribution: porphyric. gours 

Sedimentary crust fragments. Detrital gour fragments. 

Charcoals (*), herbivore excrements (**) and seeds (*). 

Calcitic crystallitic b-fabric. Amorphous yellow/black fine 

material. Pedofeatures: clay coatings (þ), Fe (hydr)oxides 

orthic nodules (þ), granular bioaggregates and roots (þþ). 

Postcardial 



CS. VIII/X.2/ 

X.4 

11, 13 

and 15 

Clayey silts and scattered Microstructure: subangular blocky, granular and platy. 25 

herbivore excrements with Fe e30% porosity. Groundmass: c/f 50 mm 1/3. Relative 

(hydr)oxides traces 

distribution: porphyric. Charcoals (***), seeds (* VIII), calcitic 

pseudomorphs (** VIII), calcitic pseudomorphs from druses 

(** CS.X.4), faecal spherulites (**), disarticulated Si 

phytoliths aggregates (*** VIII, **X.4), mineralized and 

charred herbivore excrements (**), amorphous 

phosphatized herbivore excrements (* CS.X.4), bones (**), 

light combustion bird eggshells (* CS.X.4), pottery and flint 

fragments (*). Calcitic crystallitic and undifferentiated b- 

fabric. Pedofeatures: depletion (þþ), clay coatings (þVIII 

and X.4), Fe (hydr)oxides nodules (þþþ), Fe-P hypocoatings 

(vivianite in VIII, X.2) (þþ) and granular bioaggregates (þþ). 

Hydromorphic conditions 

(vivianite). Unlaminated 

colluvium ( ), stabling areas 

traces (þ) 

Postcardial 



/ 

Epicardial 


CS. VIII/X.1 11, 12 Mineralized and charred 

erubified residues of 

herbivore excrements and 

plants in situ 

Mineralized residues. 

Stabling areas with 

Thickness: 1e6 cm. Microstructure: granular/massive. 2 combustion. 

e10% porosity. Groundmass: Crystallitic calcitic 

Hydromorphic conditions 

accumulation with some fine sands. Relative distribution: (vivianite) 

porphyric. Charcoals (*/**), prismatic pseudomorphs (***), 

droplets (**), mineralized herbivore excrements 

(ovicaprines) (**). Calcitic crystallitic b-fabric. Pedofeatures: 

granular bioaggregates (þþ/þþþ), Fe-P hypocoatings 

(vivianite) in CS.X.1 and Fe (hydr)oxides nodules (þ). 

CS. X.1 12 Charcoals residues 

Thickness: 0,5 cm. Charcoals of tabular morphology with 

woody structure. 

Charred and rubified residues 

CS. VIII/X.1 11, 12 Thickness: 1e3,5 cm. Microstructure: spongy/granular. 25 

e30% porosity. Groundmass: c/f 50 mm 1/2. Sandy silts with 

some gravel. Relative distribution: porphyric. Charcoals 

(*/**), charred fragments (**), faecal spherulites (**), 

charred/rubified herbivore excrements (**). Calcitic 

crystallitic b-fabric. Pedofeatures: Fe (hydr)oxides nodules 

(þþ) and granular bioaggregates (þþ/þþþ). 

Postcardial 



CS. XI 16, 17 Silty sands with clays with 

herbivore excremental 

aggregates 

Microstructure: subangular blocky/massive. 5e30% Unlaminated colluvium/ 

porosity. Groundmass: c/f 50 mm 2/1-1/2. Relative stabling areas traces (þ). 

distribution: porphyric. Charcoals (****), Si phytoliths (***), Hydromorphism 

faecal spherulites (***), charred herbivore excrements (**), 

bones (****) and pottery fragments (*). Calcitic crystallitic b- 

fabric. Pedofeatures: roots traces (þþ), limpid clay coatings 

(þþ), Fe (hydr)oxides orthic nodules (þ/þþþþ) and Ca 

hypocoatings (þþ). 

Late Cardial 


(continued on next page) 




10 


Table 5 (continued ) 

Can Sadurní 

Sedimentary 

layers 

Can Sadurní 


layers 



Cultural 

context 

CS. XII 18 Stones, gravels and clayey 

silts with herbivore 

excremental aggregates 

Microstructure: granular/subangular blocky. 25% porosity. Colluvium (þ)/stabling areas 

Groundmass: g/f 50 mm 3/1. Relative distribution: porphyric traces ( ) 

and chitonic. Charcoals (***), scattered faecal spherulites 

(**), Si phytoliths (***), bones (**), herbivore excremental 

aggregates (**), pottery and flint fragments (*). Calcitic 

crystallitic b-fabric. Pedofeatures: clay coatings (þ) and Fe 

dots and stainings (þ). 

Cardial 


CS. XIII 19, 20 Clayey silts with granular/ 

vesicular microstructure and 

stones 

CS. XIV 21 Clayey silts and sands with 

vesicular microstructure and 

stones 

Microstructure: granular/vesicular/subangular blocky. 20 Moderate freeze-thaw traces 

e25% porosity. Groundmass: g/f 50 mm 3/1- 1/2. Relative and solifluction 

distribution: porphyric. Stones and gravels with subangular/ 

subrounded morphology with some fissures. Inclined or 

vertical arrangement. Charcoals (**), bones (***/****). Calcitic 

crystallitic b-fabric. Pedofeatures: Fe (hydr)oxides orthic 

nodules (þ), limpid clay coatings (þþ) and dissolution 

traces in limestones. 

Microstructure: vesicular/granular/subangular blocky. 20 Solifluction 

e25% porosity. Groundmass: g/f 50 mm 4/1- 1/2. Relative 

distribution: porphyric. Charcoals (**/***), bones (**/****) 

with light traces of combustion. Calcitic crystallitic b-fabric. 

Pedofeatures: limpid clay coatings (þþþþ/þþþþþ), 

dissolution traces in limestones and bones (þþþþþ), P-Ca 

hypocoatings (þþþþþ), Fe (hydr)oxides orthic nodules 

(þþ) and granular bioaggregates (þþ/þþþ). 

Mesolithic 


The lithological and mineralogical fraction consists mainly of micritic limestone, quartz, feldspar, plagioclase and calcite. 

Class frequencies after (Bullock et al., 1985): * Very few (70%). 

Class abundance of pedofeatures after (Bullock et al., 1985): þ Rare (20%). 

replacement of the calcite by apatite (Karkanas and Goldberg, 

2010). They are indicator characteristics of the oscillating humidity 

conditions typical of these records. 

Disruptions in sedimentation are documented by biological 

activity. 

CS.XIII is distinguished especially by a granular microstructure, 

with slight fissures of the detrital material and with orientation 

changes (vertical or sloping) of bones, charcoals and some of the 

stones of subangular and subrounded morphology (Fig. 5d), indicators 

of a moderate freeze-thaw process (Van Vliet-Lano€e, 2010) 

that would cause cryoturbation processes. These characteristics 

indicate a significant change in the environmental conditions of the 

cave, which undoubtedly suffered the effects of frost once the cavity 

had been occupied. 

4.1.2. Gravitational and colluvium processes 

These processes are responsible for most of the detrital sedimentary 

record of the two cavities. Three types are distinguished, 

and in the Neolithic sequence there are also contributions of anthropic 

origin: unlaminated colluvium with gravitational movements, 

colluvium blocks and unlaminated colluvium where the clay 

silt matrix predominates in relation to the coarse fraction. 

4.1.2.1. Unlaminated colluvium with gravitational movements. 

These are distinguished in the Epipaleolithic sequence of Guineu 

(G. IIIa 12.7e12.2 and 11.5e11.1 cal ka BP). These deposits are 

characterized by their matrix of silts and clays with sands together 

with heterometric blocks of subangular morphology without internal 

ordering. The matrix and the wet conditions have been 

determinant for the placement of the level. 

The general subangular blocky microstructure is indicative of 

wetting and desiccation of the matrix (Fitzpatrick, 1990). As 

pedofeatures, as in CS. XIV there are mainly traces of clay 

illuviation. 

4.1.2.2. Colluvium and blocks. These are distinguished by the 

presence of heterometric detrital deposits with blocks and some 

angular stones resulting from collapses that were deposited in 

cavities by the retreating openings to the exterior or from the slope 

or dip slope of the karstic surface, creating gravitational debris 

cones. 

In the exterior part of Guineu there are large blocks resulting 

from the collapse of the roof of the cavity. In contrast, in Can 

Sadurní the cone is of greater amplitude and consists of clasts 

originating from the outside. The roof of Can Sadurní, however, 

presents no erosive signal, but the dissolution modelling corresponds 

to the processes of cavitation in a duct flooded by water that 

corresponds to a stage preceding the formation of the Holocene 

deposit. The anthropic alteration of the entrance of the cavity is 

very important and hides the lateral relation of the materials and 

the geometry of the deposit towards the outside. 

These detrital deposits are formed by different dry avenues that 

created debris cones towards the interior of the cavity; the first and 

the oldest having a greater slope than the more recent ones. 

They are mainly developed in the following levels of Can 

Sadurní and Guineu: CS.XII (Cardial Early Neolithic, 7.4e7.2 cal ka 

BP), CS.IX (Early Postcardial Middle Neolithic, 6.8e6.3 cal ka BP), CS. 

VII (Late Postcardial Middle Neolithic, 6.2e5.7 cal ka BP), G.II 

(Postcardial Middle Neolithic) and G. Id (Late Postcardial Middle 

Neolithic, 6.3e5.9 cal ka BP). 

It is very difficult to discern which process triggered the great 

contribution of blocks and stones since most are part of the colluvium 

filling. In any case, we consider hypotheses that could be the 

result of denudation processes of a previous phase of alteration, 

formation of collapse dolines, evolution of karren at depth and very 

intense dissolution in more humid and temperate conditions than 

the present ones. The morphology of the karren indicates an origin 

under a pedologic coverage and later retouch under aerial 

conditions. 





Table 6 

Synthesis of the micromorphological analysis description of the Cova de la Guineu. 


Sedimentary 

layers 



G. Id Stones, clayey silts with sands Microstructure: granular. 25% porosity. Groundmass: g/f 50 mm 2/ 

1.Relative distribution:porphyric. Charcoals (**), bones (*) with light 

traces of combustion. Calcitic crystallitic/undifferentiated b-fabric. 

Amorphous black organic fine material/puntuaction organic matter. 

Pedofeatures:clay coatings/hypocoatings (þþ), granular bioaggregates 

(þþþþþ) and roots. 

Colluvium, block 

breakdown and 

pedogenesis (organic 

material) 

G. Ie Sandy clays with stones Microstructure: granular/subangular blocky. 10e20% porosity. 

Groundmass: g/f 50 mm 1/3. Relative distribution: porphyric. Charcoals 

(***), bones (*) with light traces of dissolution. Calcitic crystallitic b- 

fabric. Pedofeatures: limpid clay coatings/hypocoatings (þþ), traces of 

dissolution in dolomitic limestones (þ), Fe (hydr)oxides nodules (þ) and 

bleached mottles (þ). 

Unlaminated colluvium 

and variable 

hydromorphism 

Cultural 

context 

Late 

Postcardial 



Late Cardial 


G.IIb 

Mineralized and charred erubified Mineralized residues. Units:1, 4, 6 and 8. Thickness 1e4,5 cm. Stabling areas with 

residues of herbivore excrements and Microstructure: massive. 2e10% porosity. Crystallitic calcitic 

combustion 

plants in situ 

accumulation with some fine sands. Relative distribution: porphyric. 

Charcoals (*), prismatic pseudomorphs (****), droplets (**), mineralized 

herbivore excrements (ovicaprines) (**) and pottery fragments (*). 

Calcitic crystallitic b-fabric. Pedofeatures:granular bioaggregates (þ), Fe 

nodules, dots and stainings (þ). 

Charred and rubified residues. Units: 2 and 7. Thickness 1e2,5 cm. 

Microstructure: spongy/granular. 25e30% porosity. Groundmass: c/f 

50 mm 1/2 sandy silts. Relative distribution: porphyric. Charcoals (**/***), 

charred fragments (**), faecal spherulites (**), charred/rubified herbivore 

excrements (**) and bones (*). Calcitic crystallitic b-fabric. Pedofeatures: 

Ca hypocoatings (þ), Fe dots and stainings (þþ) and granular 

bioaggregates (þþþ). 

Postcardial 



G.IIb Sandy silts Units: 3 and 5. Thickness 2,5 - 4 cm. Microstructure: granular. 25% 

porosity. Groundmass: g/f 50 mm 2/1.Relative distribution: porphyric. 

Charcoals (***), bones (*) with light traces of combustion. Calcitic 

crystallitic b-fabric. Pedofeatures: clay coatings (þþ), Ca coatings/ 

hypocoatings (þ) and granular bioaggregates (þþ). 

Diffusse runoff 

Postcardial 



G. II Sandy silts with clays and stones with 

subrounded anthropic components 

Microstructure: subangular blocky. 30% porosity. Groundmass: c/f 50 mm Colluvium 

1/2. Relative distribution: porphyric. Charcoals (***), charred and 

mineralized herbivore excrements (**), prismatic pseudomorph 

aggregates (**), bones (**), pottery fragments (**) and malacological 

remains (*). Calcitic crystallitic b-fabric. Pedofeatures: clay hypocoatings 

(þ), Ca hypocoatings/coatings (þþ), Fe dots and stainings (þ) and 

granular bioaggregates (þþþ). 

G. IIIa Stones and sandy silts with clays Microstructure: subangular blocky. 15% porosity. Groundmass: c/f 50 mm 

2/1. Relative distribution: porphyric. Charcoals (*) and bones (*) with 

light traces of combustion. Calcitic crystallitic b-fabric. Pedofeatures: 

clay coatings/hypocoatings (þþþ), Ca hypocoatings (þ), Fe dots and 

stainings (þ) and granular bioaggregates (þþþ). 

Unlaminated colluvium 

with gravitational 

movements 

Postcardial 




The litological and mineralogical fraction consists mainly of dolomitic limestone, quartz, calcite, dolomite and feldspar. 

Class frequencies after (Bullock et al., 1985): * Very few (70%). 

Class abundance of pedofeatures after (Bullock et al., 1985): þ Rare (20%). 

This type of contribution begins in the case of Can Sadurní in 

CS.XII and in Guineu by the present data in G. II. This implies the 

formation of the debris cone and the entrance of detrital materials 

occurred in the later stages. 

In Can Sadurní, the largest clasts of CS. XII are deposited with the 

longest axes parallel to the slope, together with very angular 

gravels indicating a particularly dry and cold period. There is 

stratigraphic discontinuity with respect to CS. XIII (Mesolithic). On 

the other hand, from 6.8 to 6.3 cal ka BP, the blocks and stones 

(CS.IX) are arranged with the longest axis perpendicular to the 

slope, indicating a movement in more humid conditions; in erosive 

contact and with a shallower slope than during the Cardial 

Neolithic. Along the temporal period that represents the whole 

deposit, there are pauses and reactivations that cause a replacement 

of coarse fraction and redistribution of the finer ones, 

especially towards the more distal parts. 

This last episode correlates with G. II (Postcardial Middle 

Neolithic), presenting an erosive contact with G. IIIa (Epipaleolithic). 

This process also recurred during 6.2e5.7 cal ka BP in 

Can Sadurní (CS VII - VI) with an erosive contact, and in Guineu (G. 

Id). In this latter cave, two great blocks that were detached from the 

roof are located in the top wall of the level. 

From the micromorphological point of view they are characterized 

by a groundmass rich in the coarse fraction, with little internal 

cohesion. It consists of mixed bone and malacological 

remains, charcoals, pottery and a few excremental aggregates of 

ovicaprids (Fig. 5e). The microstructure is weak granular/subangular 

blocky, with traces of material rotation, characteristic features 

of these records (Bertran and Texier, 1999; Karkanas and 

Goldberg, 2013). In Guineu, G. Id, an enrichment of organic 




12 


Fig. 5. Micromorphological features of the pedosedimentary processes in the sites located between c. 13.0e6.0 cal ka BP. 

a. Can Sadurní. CS.XIV. Vesicular microstructure. Vesicle voids (v). PPL. 

b. Can Sadurní. CS.XIV. Fine material hypocoating with oriented domains (arrow) in a void. XPL. 

c. Can Sadurní. CS.XIV. Traces of very sharp dissolution in bone fragment (arrow). In the interior, a fine hypocoating can be observed. PPL. 

d. Can Sadurní. CS.XIII. Vertically oriented coarse material: gravels and charcoal fragments. PPL. 

e. Guineu. G.II. Subrounded pottery (P) fragment together with a burned ovicaprine coprolite (C) and subrounded morphology wood ash aggregates mixed in the groundmass (A). 

PPL. 

f. Can Sadurní. CS.X. Phosphatic accumulations in excremental aggregate with the presence of vivianite (v). XPL. 

g. Can Sadurní.CS.VIII. Field view of a gour fragment (arrow). 

h. Can Sadurní. CS.VIII. Gour groundmass. Note microsparitic calcite hypocoating (arrow) in the top of the gour. 





Fig. 6. Stabling area with combustion (layer cake). Guineu (G.IIb): micromorphological features. 

a. General view. At the top, mineralized residues appear and at the bottom, rubified and charred residues. 

b. Detail of the previous image. 1. Ash accumulation composed of calcite pseudomorph of plant origin with some charcoal fragments and ovicaprine mineralized coprolites. 2. 

Charcoals (arrows) charred and rubified droppings. XPL. 

c. Detail of a burned ovicaprine coprolite. Note the presence of the carbonized organic coating covering the faecal spherulites (arrow). XPL. 

d. Detail of wood ashes (prismatic calcitic pseudomorphs) (arrows). PPL. 

e. Detail of charred and rubified dropping. In arrow faecal spherulithes. 

XPL. 

matter is visible in the exterior sector. It is characterized by intense 

biological activity, mainly of roots as documented both by the 

channel microstructure and by the presence of their remains. This 

corroborates its aerial exposure for an extended period of time. 

4.1.2.3. Unlaminated colluvium. This is characterized by a fine matrix 

of clayey silt; in places there is a significant increase in the 

sandy fraction, along with some stones and scattered blocks. From 

the micromorphological point of view they are characterized by a 

massive/subangular blocky microstructure with a very fine separation 

between the aggregates, common traces in these contexts 

(Mücher et al., 2010). Components of anthropic origin also appear 

dispersed in the groundmass. 

In some levels sedimentary contributions are weak and so human 

activity is better reflected and the removal of its components is 

lower. This is the case of CS. XI (Late Cardial Neolithic) and CS.X 

(Epicardial Neolithic) dated between 7.2 and 6.6 cal ka BP, G.Ie (Late 

Cardial Neolithic, 7.1e6.9 cal ka BP) and CS.VIII (Postcardial Middle 

Neolithic, 6.5e5.9 cal ka BP). In others, there is an increase in the 

sandy fraction, anthropic components are less conserved and are 

removed as in some microfacies of CS.XI (Late Cardial Neolithic). 

Among the most common pedofeatures are: 

- Eluviation/illuviation. This is generally present and is typical of 

this type of context where water infiltrates and involves a 

percolation of fine material (clay) that is then retained in the dry 

voids of the lower levels (Fernandez et al., 2015). 

- Hydromorphism features. These occur in nodules of iron oxides 

and hydroxides and in rare cases of manganese, and have a 

special importance in the sequence of the Late Cardial Neolithic, 

Epicardial until the Postcardial Middle Neolithic from Can 

Sadurní. They are indicators of water saturation, mainly temporary 

or deficient drainage, and coincide with the increase of 

pastoral activity in the interior of the cave. 

An interesting feature is the presence of vivianite in Can Sadurní 

(Fig. 5f). Reducing conditions and abundant availability of iron and 

phosphorus are required for its formation (McGowan and 

Prangnell, 2006; Karkanas and Goldberg, 2010). In our case, its 

genesis is the result of the abundance of residues rich in phosphate 

(excrement and plant matter) in a reducing context (Nicosia, 2008). 

In Guineu, in the Late Cardial Neolithic (G. Ie), oxide and hydroxide 

nodules are observed and there are bleached mottles 

characteristic of a variable hydromorphism in reducing conditions 

(Dorronsoro et al., 2015). 




14 


- Biological activity. Especially roots, in voids, features that indicate 

surface exposure in some episodes; and where calcitic 

hypocoatings appear in root biopores as a result of the rapid 

precipitation of calcium carbonate due to root metabolism 

(Durand et al., 2010). 

4.1.2.4. Diffuse runoff. This process is not generalized and is located 

in the Postcardial Middle Neolithic in Can Sadurní (CS.VIII, 

6.5e5.9 cal ka BP) and in Guineu (G.IIb, 6,4e5,9 cal ka BP). It is 

characterized by the sedimentation of silty clays and sands in an 

environment of very low energy; in others, the runoff is more active 

with the formation of sedimentary crusts. 

In the wall of the SE sector of Can Sadurní (CS.VIII, 6.5e5.9 ka BP) 

staggered gours follow the slope of the wall, in contact with the 

sedimentary deposit of the cavity (Fig. 5g). These are very similar in 

morphology to lithochemical gours but have a matrix of silts and 

dark clays with sands. The microstructure is massive, with some 

traces of carbonates (Fig. 5h). They have been formed by the 

percolation of water from the wall of the cavity, which leaches the 

fine sediment deposited on it. The fine sediment accumulates in a 

fine corrugated line of small puddles created from the irregularities 

of the floor and where the slope weakens. The repetition, perhaps 

seasonal, of this phenomenon causes the wall to grow without 

erosion, thus the dam increases its height and thickness for new 

contributions of water with a new load of muddy sediment. The 

continuity of the growth without the erosion breaking the form is 

because the water never surpasses laminar slip-flow. When the 

gours are well formed they are staggered downwards and the lower 

ones receive the water from the overflow of the higher ones. This 

has a regulating and laminating effect on the flow and guarantees 

the continuity of the process. They mark a stable episode inside the 

cavity. 

4.2. Anthropic sedimentation located between c. 7.4e6.0 cal ka BP 

The sedimentation generated by the human activity of this 

period is closely related to stabling practices, mainly ovicaprids, in 

the studied sites. Different types of contributions are located: 

4.2.1. Clayey silts with sands and stones with herbivore excremental 

aggregates and phosphated inclusions 

The evidence is found in Can Sadurni, in the Early Cardial 

Neolithic between 7.4 and 7.2 cal ka BP (CS.XII, layer 18). It is 

notable for the presence of faecal calcium spherulites (Canti, 1997) 

in the groundmass. Also, there is an appearance of excremental 

aggregates that because of their composition and internal fabric 

may be from ovicaprines (Courty et al., 1989; Bergada, 1998; Polo 

Díaz, 2010). Diagnostic components of this activity are scarce and 

spatially very dispersed which leads us to suggest that some ovicaprid 

stabling has occurred (Bergada and Cervello, 2011; Bergada 

et al., in press). They are comparable to other Mediterranean records 

of similar chronologies (Angelucci et al., 2009). It should also 

be added that colluvial reactivations and the sepulchral use 

(Antolín et al., 2011a) could have contributed to the dispersal of the 

remains of these occupations. 

During the Late Cardial Neolithic and Epicardial in Can Sadurni 

between 7.2 and 6.6 cal ka BP (CS.XI, layers 17 and 16 and CS X 

layers 15, 14, 13) the presence of these components increases, 

although they are still spatially dispersed. Some of the excrements 

appear with slight traces of combustion. Also, the calcitic 

pseudomorphs (druses), which are indicators of ash, present 

varying morphologies, more or less spherical that according to 

Brochier (1996) are more commonly found in leaves of woody 

materials. In addition, phytoliths of silica of varied morphologies 

appear. 

The sedimentary contributions are of lower intensity, which 

favours their preservation in the sedimentary record. Remains of 

bird eggshell are also located in the groundmass, which demonstrates 

that there were phases of abandonment in Can Sadurní that 

would have been used by the birds to nest (Bergada et al., in press). 

Regarding Guineu (G.Ie), at the moment, remains of pastoral activity 

have not been documented, but only a sector of 4e5m 2 in the 

exterior of the cave has been excavated to date. 

4.2.2. Mineralized and charred erubified residues of herbivore 

excrements and plants in situ 

These are located during the Postcardial Middle Neolithic corresponding 

to Can Sadurní, c. 6.6e5.9 cal ka BP (CS.X, layer 12 and 

CS.VIII layer 11) and in Guineu, c. 6.4e5.9 cal ka BP (G. IIb). The 

detrital sedimentation decreases markedly and there are areas with 

combustion, which are characterized by the following sequence of 

microfacies (from top to bottom): 

1. Mineralized residues (ash). Among the components are: excremental 

aggregates, calcitic pseudomorphs (druses and prisms) 

(Canti, 2003) and rounded micritic residues called droplets 

(Courty et al., 1989; Polo Díaz, 2010). The prismatic pseudomorphs 

correspond, as druses, to the remains of woody plants; 

although the prisms are in the bark and the druses in the leaves 

(Brochier, 1996). The droplet micritical residues are the result of 

a very high combustion of the vegetal remains (Courty et al., 

1989; Polo Díaz, 2010). 

2. Woody charcoal residues (in some cases this microfacies is 

located in Can Sadurní). 

3. Charred and rubified residues. It consists mainly of charred and 

rubified excremental and plant fragments, amorphous yellow 

phosphated accumulations and organic fine material. 

These accumulations recorded in Can Sadurní and Guineu 

(Bergada et al., 2005a and Bergada et al., in press) (Fig. 6a and b), 

have been referred to as a layer-cake stratigraphy (Macphail et al., 

1997). Once the animals leave the cavity, the excremental residues 

are exposed at the surface and after that, burning would occur 

at a low temperature and in reducing conditions (Fig. 6b and e) e 

microfacies 3 -. The presence of an upper layer e microfacies 1- 

mostly formed by woody plants (Fig. 6d) and by some excrements 

(Fig. 6c) in such cases, the combustion would have been more 

ventilated and at a higher temperature; the fact that woody charcoals 

are located (microfacies 2) would correspond to the same 

episode but with less ventilation. The accumulation of woody remains 

from the stable structure or from remains of tree branches 

that would have served as food for livestock (Bergada et al., in 

press). 

The reason for these burning practices may lie in a need to clean 

up the place, once the occupation is restarted as has been documented 

in other records (Angelucci et al., 2009; Bergada et al., 

2005b; Courty et al., 1991; Macphail et al., 1997; Polo Díaz, 2010; 

Polo Díaz et al., 2014; Verdasco, 2016). This practice has also been 

documented experimentally (Verges et al., 2016) and ethnographically 

(Verdasco, 2016). 





Fig. 7. Stabling area without combustion. Can Sadurní (CS. VIII): micromorphological features. 

a. Layers of disarticulated silica phytoliths with a fine organophosphate groundmass, slightly compacted next to a dung (D). PPL. 

b. Same as (a) in XPL. Undifferentiated b-fabric is distinguished in the phosphated area with silica phytoliths. 

c. See in detail the silica phytoliths (arrows). PPL. 

d. Fragment of bovine coprolite. Note the articulation of phytoliths inside (arrow). PPL. 

e. Same as (d) in XPL. 

These areas with combustion alternate with others without 

combustion, especially in Can Sadurní. It is common of this type of 

deposit and has also been described in other Neolithic Mediterranean 

records in caves and rockshelters (Angelucci et al., 2009; 

Boschian, 2006; Boschian and Miracle, 2007). Although for the 

moment its interpretation is complex, it has been suggested that it 

may be the result of the alteration and trampling of unburned or 

partially burned stabling areas (Boschian, 2006), also as a product 

of very irregular combustion (Brochier, 2002) or of domestic activities 

simultaneous to or between this pastoral activity (Bergada, 

1997; Polo Díaz, 2010; Egüez et al., 2016). 

4.2.3. Layers of phytoliths and organophosphated herbivore 

excrements in situ 

In some sectors of Can Sadurní, such as in F-9 (CS.VIII layer 11) 

and the Postcardial Middle Neolithic, layers have been located 

consisting of articulated and disarticulated phytoliths of varied 

morphologies with a fine organophosphated groundmass (Fig. 7a, b 

and 7c) and coprolites which correspond in composition and internal 

fabric most likely to cattle (Fig. 7d and c) (Bergada, 1998; Polo 

Díaz, 2010) and others to ovicaprines (Bergada et al., in press). 

These accumulations represent a pattern different from the previous 

one, with vegetal, excremental accumulations or a combination 

Fig. 8. Cumulated probability curves obtained from the CalPal2007- Hulu calibration of the dates coming from Cova de Can Sadurní and Cova de la Guineu compared with the d 18 O 

variation curves obtained in the NGRIP and GRIP cores, following the GICC05 Age Model (Lowe et al., 2008). It is observed as from c. 12.7e7.4 cal ka BP there is a great discontinuity 

in the recorded caves dominating the hiatus phases. From c. 7.4e6.0 cal ka BP there is a certain continuity in the sequence and climatic variability. 




16 


Table 7 

Chronostratigraphy in karst records from Epipaleolithic to the Mid/Early Neolithic (c. 13.0e6.0 cal ka BP) in the Catalan Coastal Ranges: Cova de Can Sadurní and Cova de la 

Guineu. In gray, the recorded sedimentary episodes; in orange, the episodes where a detrital sedimentation dominates with collapses and debris cones of an arid environment 

and, in blue, episodes where anthropic sedimentation dominates in a humid and stable environment. Can Sadurní (S) and Guineu (G). 

Age 

yr BP 

Pedosedimentary and anthropic processes 

Can 

Sadurní 

VII-VI 

(10 - 10b) 


Palaeoenvironment 

cal ka BP 

Cultural sequence 

Late Postcardial Middle 


6.000 

Colluvium and clastic dejection. High energy. Erosive contact (S/G) 

Id Arid ( c.6.2 - 5.7) 

Stabling area/Layer cake (S/G) 

X-VIII 

Humid (stability in the Postcardial Middle 

IIb 

Diffuse runoff (S/G) / gours with high detrital component (S) (12 - 11) 

environment) (c. 6.6 - 5.9) Neolithic 

Colluvium and clastic dejection. High energy. Erosive contact (S/G) IX (11b) II Arid (c. 6.8 - 6.3) 

Hydromorphism (S) ? 

Epicardial and Late 

7.000 Humid (c. 7.1 - 6.7) 

Cardial Neolithic 

Unlaminated colluvium (S/G), Stabling area (+) (S) XI-X (17-13) Ie 

Colluvium and clastic dejection. High energy. Stabling area (-) (S) XII (18) ? Arid (c. 7.4 - 7.2) Cardial Neolithic 

8.000 

Hiatus Hiatus Hiatus Hiatus 

Solifluction processes/cryoturbation XIII (20-19) Less humid (c. 8.2 - 8.0) Mesolithic 

9.000 

Hiatus Hiatus Hiatus Hiatus Hiatus 

10.00 

(c. 10.7 - 10.4) 

XIV (21) 

Fine material colluvium with gravitational movements/Solifluction 

11.00 Fresh and humid Epipaleolithic 

processes 

IIIa (c.11.5 - 11.1) 

12.00 Hiatus Hiatus Hiatus 

Fine material colluvium with gravitational movements/Solifluction 

processes 

(c. 12.7 - 12.2) 

XIV (21) IIIa Fresh and humid Epipaleolithic 

of both in the form of beds without traces of combustion. It should 

be noted that they exhibit some scattering due to the diffuse runoff, 

trampling effects and biological activity. 

We propose that the combustion would occur in the accumulations 

where woody debris would be present. Episodes of abandonment 

have also been detected, characterized by the presence of 

eggshell fragments indicating birds nesting in the cave. 

5. Discussion 

5.1. Are there any chronostratigraphic discontinuities during the 

Epipaleolithic and Mesolithic? 

In the studied caves during c. 12.7e7.4 cal ka BP several stages of 

hiatus are distinguished and are reflected in the following episodes 

(Fig. 8 and Table 7): 

- c. 12.7e11.1/10.4 cal ka BP 

This episode would coincide with the Younger Dryas and the 

start of the Holocene. In general, YD has been widely recognized in 

different proxies in Iberia and has a tendency towards cold and 

relatively arid conditions (Bartolome et al., 2012; Cacho et al., 2010). 

In our records, there is a dominance of solifluction and colluvial 

deposits of fine and gravitational material in fresh and humid 

conditions. This agrees with the archaeobotanical and faunistic 

data of Can Sadurní (Antolín et al., 2011b, 2013) and there is a hiatus 

between 12.2 and 11.5/10.7 cal ka BP. 

In the stratigraphic and sedimentary sequences of caves and 

rockshelters of the Mediterranean basin and Ebro valley, cold/fresh 

episodes are documented (Angelucci, 2005; Aura et al., 2011; 

Bergada, 1998; Ferrer, 2015; García-Argüelles et al., 2013 Montes 

et al., 2016), some with erosive events (Aura et al., 2011). In the 

north-east of the Iberian Peninsula there is generally a hiatus that 

coincides with the second half of the YD and the start of the Holocene 

(García-Argüelles et al., 2013) corresponding to the records 

analyzed in this paper (Fig. 9). 

This interruption could be related to the phase of increased 

humidity observed in speleothem records that would have allowed 

the advance of the glaciers in the northern Iberian mountains 

(García-Ruiz et al., 2016). On the contrary, in other areas such as 

Arba de Biel in the Ebro Valley, an occupation gap (Montes et al., 





Fig. 9. Stages of discontinuities referenced on the basis of the data obtained from Iberian NE archaeological sites, mentioned in the text, from their probability curves obtained from 

the CalPal2007- Hulu calibration, compared with the d 18 O variation curves obtained in the NGRIP and GRIP cores, following the GICC05 Age Model (Lowe et al., 2008). We observe 

that in the second half of Younger Dryas there is a generalized hiatus with the exception of Parco and Cativera and sedimentary episodes and human occupations are presented in a 

more fragmented way during Early Holocene. 

2016) is detected between 12.2 and 10.1 cal ka BP, linked only to a 

cultural strategy of territorial use and not to an episode of depositional 

hiatus. 

This change in the environment that is reflected in the second 

half of the YD and Preboreal could have contributed to the very 

uneven Epipaleolithic occupation registered in different contexts 

and geographical areas. 

- c. 11.1/10.4e7.4 cal ka BP 

This coincides fully with the Holocene Climatic Optimum 

(Morellon et al., 2009) although it appears apparently synchronous 

in different records of Iberia, the climatic conditions were not 

reached at the same time (Moreno et al., 2012) and there are differences 

between the northern and southern areas as mentioned in 

the introduction. Rapid climatic changes (RCCs) begin to manifest 

at early dates in different types of records and both lacustrine and 

karst speleothems (Burjachs et al., 2016; Moreno et al., 2013; Perez- 

Sanz et al., 2013). 

In the studied caves, this stage is characterized by a phase of 

hiatus that is interrupted in Can Sadurní by the sedimentary 

episode CS.XIII dated 8.2e8.0 cal ka BP. In the pollen studies of cores 

near our study area, subhumid climatic conditions occur between c. 

10.7/8.9 and 7.9 cal BP, although in the Garraf massif vegetal thermophilic 

communities begin to appear, which would demonstrate 

the initiation of Mediterranean climatic conditions during this time 

(Riera et al., 2007). 

In sites, generally caves and rockshelters, of NE Iberia between 

c.11.1/10.4e8.2 cal ka BP there is a variability of sedimentary contributions 

marked by stages of discontinuities that mostly respond 

to hiatuses (Fig. 9). In Cova del Vidre (Tarragona) and Cova del Parco 

(Lleida) these gaps are generalized during this period (Bergada, 




18 


1998); in others, there are occasional episodes of detrital inputs 

characteristic of wet, fresh or arid contexts as in Balma del Gai 

(Barcelona), Abric del Filador y Molí del Salt (Tarragona) (Bergada, 

1998; García-Argüelles et al., 2013; Vallverdú and Carrancho, 

2004); some are also characterized by a beginning of pedogenesis 

with carbonation processes as in Abric de la Cativera (Tarragona) 

(Angelucci, 2005) or travertinization in Font del Ros (Barcelona) 

(Jorda et al., 1992) or by stalagmite formation in Cueva de Seso 

(Huesca) (Bartolome et al., 2012). One aspect that we would like to 

emphasize by the documented data is that perhaps the rockshelters 

may be a type of record that better reflects the sedimentary and 

palaeoenvironmental variations of this stage. 

A solifluction level (c. 8.2e8.0 cal ka BP) is located in Can 

Sadurní, in a less humid environment with slight traces of cryoturbation 

that could be related to the global event of 8.2 Ka cal BP 

with a tendency to cold and arid conditions. At the same time between 

c. 8.4 and 7.9 cal BP in the Delta del Llobregat near the site, 

the existence of pre-Neolithic fires with a brief climatic oscillation 

of drier conditions towards c. 7.9 cal BP has been demonstrated 

(Riera et al., 2007). 

This event is not very well represented in the Iberian Mediterranean 

basin in rockshelters and caves; but some dated 

around this event are characterized from a sedimentary point of 

view by an arid environment, such as Tossal de la Roca and Abric 

de la Falguera, both in Alicante (Cacho and Jorda, 2009; García- 

Puchol and Aura, 2006), or by a clear truncation episode, an 

erosive phase, such as the Balma Margineda rockshelter (Berger 

and Guilaine, 2009). These traits would coincide at the human 

level with the pre-Neolithic gap (Morales and Oms, 2012) or 

archaeological silence (Gonzalez-Samperiz et al., 2009). The latter 

authors attributed this to environmental conditions being 

unfavourable for habitability in some areas. It is noteworthy that 

in this episode there is a tendency to a cultural gap in the 

Mediterranean from Greece to Iberia (Berger and Guilaine, 2009). 

Therefore, it seems that a change in the distribution pattern of 

human occupation coincides with the c. 8.2 cal ka BP event, with 

paleoecological and palaeoenvironmental implications of great 

importance. 

Towards c. 8.0e7.4 cal ka BP, at the transition between the 

Mesolithic and the Neolithic, most records of continental and marine 

continuous sequences of Iberia experienced conditions tending 

to aridity, as indicated in the Introduction. In other contexts a climatic 

variability is observed, such as in the river records of the 

middle Rhone valley where stability episodes dating from 8.05 to 

7.7 ka and others with a high hydrological activity dating to 

7.7e7.49 ka are located (Berger et al. al., 2016). 

In Can Sadurní and Guineu, it is difficult to verify this episode 

because it is also represented by another hiatus phase, coinciding 

with other cavities such as Cova d'en Pardo (Ferrer, 2015) and Cova 

del Vidre (oral communication Dr. Josep Bosch). There are data 

based on the study of speleothems in the Cueva de los Molinos 

(Teruel) through the analysis of stable isotopes (d 18 O and d 13 C) and 

trace elements of speleothemic carbonate (Moreno et al., 2013), 

which indicate the existence of two events dated 8.2 and 7.4 ka that 

are interpreted as cold and very humid, typical of an environment 

with a very dense vegetation cover. 

Together, these data allow us to develop the hypothesis that, 

despite this being a complex stage and marked in some records by 

climatic variability, the signals reflected in the cavities, during c. 

12.7e7.4 cal ka BP are those representing episodes of some stability. 

This could also correspond to an environment lacking seasonal 

acute episodes; which would explain the interruptions in 

detrital contributions into the interior of the caves at the analyzed 

sites. 

5.2. Are there any episodes of climatic variability in caves from the 

Early Neolithic period onwards? 

The geoarchaeological and microstatigraphic study of the cavities 

that are the object of our study reveals that from c. 7.4 to 6.0 cal 

ka BP there was a certain chronostratigraphic continuity (Fig. 8) 

with a series of successive sedimentary processes mainly of the 

detrital and anthropic type that are expressed in episodes of short 

duration (Table 7). From these we highlight: 

a) Detrital sedimentation formed by collapses that involved the 

formation of debris cones and the entrance of detrital materials 

in mass, with blocks and stones, typical of an arid environment, 

with colluvium reactivations. 

They have been identified in different episodes: 

- from 7.4 to 7.2 cal ka BP corresponding to the Cardial Early 

Neolithic in Can Sadurní (CS. XII, layer 18). 

- from 6.8 to 6.3 cal ka BP corresponding to the Early Postcardial 

Middle Neolithic in Can Sadurní (CS IX, layer 11b) and probably 

in Guineu (G. II) 

- from 6.2 to 5.7 cal ka BP corresponding to the Late Postcardial 

Middle Neolithic in Can Sadurní (CS.VII-VI, layer 10b and 10) and 

Guineu (G. Id) 

These episodes would be in accordance with the proposal of 

Wanner et al. (2011) on a global scale in which he identified a more 

recent phase of Bond 5 (5a) dated around 7.5 cal ka BP and located a 

concentration of dry events between the 7.2e5.7 cal ka BP. 

In these episodes, the one that corresponds to the Cardial Early 

Neolithic compares the best with other sites in other zones of Iberia 

as well as the Levante area, where the processes of mass movement 

and colluviation have caused fillings in the slopes and caves (Ferrer, 

2015; Fumanal, 1995). 

Fire episodes were located in the pollen core from the Delta del 

Besos in Barcelona, an area close to our studies, (Riera et al., 2007), 

as well as in the Rhone middle valley (Berger et al., 2016) where 

intense peaks of localized fires occurring between 7.57 and 7.32 ka 

were revealed. For Berger et al. (2016), these episodes reflect variations 

in climatic and atmospheric activity responsible for periods 

of aridity. Data coinciding with the contributions of Vanniere et al. 

(2011) indicate that in the Mediterranean there is a synchronicity 

between the episodes of fires with the climatic droughts that were 

determinant during these stages. 

These traits indicate that the Cardial Neolithic was a stage of 

very active morphogenesis with a high probability of not being able 

to identify settlements in the open air of this stage and even earlier 

(Berger and Guilaine, 2009; Berger, 2011; Berger et al., 2016); which 

would lead us to consider that the cavities would act as sedimentation 

traps capable of retaining such contributions from the 

outside and would constitute the most favourable deposits for the 

conservation of these occupations. 

Subsequently, two events dated 6.8e6.3 and 6.2e5.7 ka cal BP 

correspond to phases of instability with reactivations of gravitational 

processes. These reactivations caused erosive contacts in the 

underlying sedimentary levels in some sectors of the cavities that in 

Guineu occurred in the Epipaleolithic level. From this stage, correlations 

with other nearby records have not yet been observed. 

b) (Less) detrital sedimentation and (more) anthropic sedimentation. 

It is located in two episodes dated c.7.1e6.7 cal ka BP corresponding 

to the Epicardial and Late Cardial periods and c. 

6.6e5.9 cal ka BP, Postcardial Middle period, the latter with 

greater representation in the sequences. The sedimentation 





generated by human activity is strongly present in the caves 

with animal stabling practices (mainly ovicaprids) in which 

levels with burnt material (layer-cake) or without are alternated. 

The environment was humid, with some stability, especially 

during the Late Cardial/Epicardial period, in which an 

increase of hydromorphic processes is detected, possibly 

reflecting non-permanent water saturation. It correlates with 

the data provided by anthracology of Guineu (Allue et al., 2009); 

as well as the palynological analyses indicating an expansion of 

wetlands in the deltaic plains of Llobregat (Riera et al., 2007). It 

also reflects the same environmental conditions during the 

Postcardial Middle Neolithic and the appearance of detrital 

gours in Can Sadurní are typical of a stable environment. 

It is at this episode that the use of the cavities for animal pens is 

recorded with good resolution, quite possibly favoured by the 

environmental conditions. Most probably this anthropic sedimentation 

is responsible for the episodes of oscillating humidity reflected 

in the sequences of the caves where, if not for this 

contribution, perhaps a hiatus would be located. On the other hand, 

the detrital contributions are smaller and this can favour the tendency 

to create palimpsests in the different occupations of the 

cavities. This is the case in Can Sadurní CS.VIII (level 11) where a 

burial phase dated 6.3e6.1 cal ka BP overlaps a stabling phase dated 

6.6e6.4 cal ka BP (Antolín et al., in press; Edo et al., in press a). 

6. Conclusions 

Holocene climatic variability is clearly reflected in caves in the 

Catalan Coastal Ranges of NE Iberia during the Middle and Early 

Neolithic. 

The detailed analysis of the sedimentary sequences of these 

caves offers data that complement the palaeoenvironmental 

studies obtained from high resolution records and especially at this 

stage, c.13e6.0 cal ka BP, in which there are considerable changes in 

ecosystems and within human communities. 

Through the geoarchaeological and microstratigraphic studies 

of the analyzed karst records we highlight two stages: 

a) c. 12.7e7.4 cal ka BP, corresponding to the Epipaleolithic and 

Mesolithic. This period is characterized by the presence of 

stratigraphic, chronological and cultural discontinuities. Episodes 

dated 12.7e12.2 cal ka BP (Younger Dryas first half), 11.5/ 

11.1e10.7/10.4 cal ka BP (beginning of the Early Holocene) and 

8.2e8.0 cal ka BP (onset of the Middle Holocene). The conditions 

are fresh and humid; although in the range 8.2e8.0 there is less 

humid. 

However, the trait characterizing this episode is the location of 

the hiatus phases - depositional pauses - indicative of biostasy 

phases or absence of seasonal acute episodes. This is corroborated 

in the caves of the NE of Iberia; as well also as a certain tendency in 

the Mediterranean area (Berger and Guilaine, 2009). 

Our opinion is that, added to these hiatuses, there is a lack of 

anthropic occupation that suggests during this period there was a 

change of strategy of the hunter-gatherer communities in the use of 

the cavities. 

b) c. 7.4e6.0 cal ka BP, corresponding to the Neolithic, is the one 

that offers the greatest resolution in the cavities. It is manifested 

in our records with an important detrital and anthropic sedimentation 

rate. 

Climate variability is recorded. There are alternating cumulative 

episodes of short duration, characteristic of the morphogenesis of 

slopes in an arid Mediterranean environment. 

These short and cyclical periods could be correlated with the socalled 

RCCs, arid events, which in our context would be the 

following: c. 7.4e7.2 cal ka BP- Cardial Neolithic; c. 6.8e6.3 cal ka 

BP- Early Postcardial Middle Neolithic and c.6.2e5.7 cal ka BP- Late 

Postcardial Middle Neolithic. 

These arid events alternate with episodes of stability that are 

more humid and coincide with a better sedimentary record of the 

pastoral activity during the Epicardial and Late Cardial Neolithic (c. 

7.1e6.7 cal ka BP) and Postcardial Middle Neolithic (c. 6.6e5.9 cal ka 

BP). 

It is interesting to emphasize from an archaeological point of 

view that the caves played an important role in the use of territory 

in Neolithic communities; they were used mainly as stabling, which 

is a great anthropic contribution to the sedimentary record. 

Acknowledgments 

This research is part of the HAR2014-55131 research project of 

the MICINN, 2014/100780 and 2014/100482 of Generalitat de Catalunya 

and the Quality Research Group of Generalitat de Catalunya 

SRG2014-108. 

References 

Alley, R.B., Mayewski, P.A., Sowers, T., Stuiver, M., Taylor, K.C., Clark, P.U., 1997. 

Holocene climatic instability: a prominent widespread event 8200 yr ago. Geology 

25, 483e486. 

Allue, E., Vernet, J.L., Cebria, A., 2009. Holocene vegetational landscapes of NE 

Iberia: charcoal analysis from Cova de la Guineu, Barcelona, Spain. Holocene 19 

(5), 765e773. 

Amigo, J., 1983. Estructura del contacte entre la Serralada Prelitoral i la Depressio 

del Penedes (Torrelles de Foix, Pontons, Font-Rubí). Report Facultat de Geologia. 

Universitat de Barcelona (Unpublished). 

Angelucci, D.E., 2005. Nuevas aportaciones sobre el límite Pleistoceno e holoceno 

en Catalu~na: los yacimientos del abric de la Cativera y de Picamoixons (Tarragona). 

In: Santonja, M., Perez-Gonzalez, A., Machado, M.J. (Eds.), Geoarqueología 

y Patrimonio en la península Iberica y el entorno mediterraneo. 

Adema, Soria, pp. 395e409. 

Angelucci, D.E., Boschian, G., Fontanals, M., Pedrotti, A., Verges, J.M., 2009. Shepherds 

and karst: the use of caves and rock-shelters in the Mediterranean region 

during the Neolithic. World Archaeol. 41 (2), 191e214. 

Antolín, F., Ache, M., Bergada, M.M., Blasco, A., Buxo, R., Edo, M., Gibaja, J.F., 

Mensua, C., Palomo, A., Pique, R., Ruiz, J., Sa~na, M., Verdún, E., Villalba, M.J., 

2011a. Aproximacio interdisciplinaria a l'accio del foc en les inhumacions i 

aixovars del Neolític antic cardial de Can Sadurní (Begues, Baix Llobregat). In: 

Blasco, A., Edo, M., Villalba, M.J. (Eds.), La Cova de Can Sadurní i la Prehistoria de 

Garraf. Recull de 30 anys d'investigacio, Begues, desembre 2008. EDAR, Milano, 

pp. 151e158. 

Antolín, F., Buxo, R., Mensua, C., Pique, R., 2011b. Vegetacio i aprofitament de 

recursos forestals al Garraf durant la Prehistoria. In: Blasco, A., Edo, M., 

Villalba, M.J. (Eds.), La Cova de Can Sadurní i la Prehistoria de Garraf. Recull de 

30 anys d'investigacio. Begues, desembre 2008. EDAR, Milano, pp. 221e226. 

Antolín, F., Pique, R., Ballesteros, A., Burjachs, F., Buxo, R., Mensua, C., Edo, M., 2013. 

Changes in the interaction between society and the environment from Mesolithic 

(10300-8500 cal BC) to the Early Neolithic (c. 5400 cal BC) in Can sadurní 

cave (Begues, Barcelona province, Spain) a view from the archaeobotanical data. 

BAR Int. Ser. 2486, 19e29. 

Antolín, F., Martínez, P., Fierro, E., Leon, M., Martínez, H., Gascon, M., Bergada, M. M., 

Prats, G., Barcelo, J.A., Edo, M., in press. Towards the periodization of the uses of 

Can Sadurní Cave (Begues, Catalonia) during the Middle Neolithic I. The 

contribution of Bayesian modelling to radiocarbon dating sequences. In: 

Barcelo, J.A., Bogdanovick, I., Morell, B. (eds.) Ibercrono. Cronometrías para la 

historia y arqueología de la Península iberica. 

Aura, J.E., Jorda, J.F., Montes, L., Utrilla, P., 2011. Human responses to younger Dryas 

in the Ebro Valley and mediterranean watershed (eastern Spain). Quat. Int. 242, 

348e359. 

Bartolome, M., Moreno, A., Sancho, C., Hellstrom, J., Belmonte, A., 2012. Cambios 

climaticos cortos em El Pirineo central durante El final del Pleistoceno superior 

y Holoceno a partir del registro estalagmítico de la cueva de Seso (Huesca). 

Geogaceta 51, 59e62. 

Bartrina, M.T., Cabrera, L.L., Jurado, M.L., Guimera, J., Roca, E., 1992. Cenozoic evolution 

of the central catalan margin (Valencia Trough, western mediterranean). 

Tectonophysics 203, 219e248. 

Bartrolí, R., Bergada, M.M., Cebria, A., Fontugne, M., 1992. El model microlaminar 

geometric a la Catalunya meridional: aportacions del projecte d’investigacio de 

la Serra de Font-Rubí (Alt Penedes). 9e Col.loqui Internacional d'Arqueologia de 




20 


Puigcerda. Estat la Investig. sobre el Neolític Catalunya, Andorra, pp. 34e37. 

Benyarku, C.A., Stoops, G., 2005. Guidelines for Preparation of Rock and Soil Thin 

Sections and Polished Sections. Department of Environment and Soil Science, 

University of Lleida, Lleida. 

Bergada, M.M., 1997. Actividad antropica en el Neolítico antiguo catalan a traves del 

analisis micromorfologico. Trab. Prehist. 54 (2), 151e162. 

Bergada, M.M., 1998. Estudio geoarqueologico de los asentamientos prehistoricos 

del Pleistoceno Superior y el Holoceno inicial en Catalunya. BAR International 

Series 742. Archaeopress, Oxford, p. 267. 

Bergada, M.M., Cervello, J.M., 2011. Estratigrafia, micromorfologia paleoambient de 

la Cova de Can Sadurní (Begues, Baix Llobregat) des dels c. 11.000 fins els 5.000 

anys B.P. In: Blasco, A., Edo, M., Villalba, M.J. (Eds.), La Cova de Can Sadurní i la 

Prehistoria de Garraf. Recull de 30 anys d'investigacio. Begues, desembre 2008. 

EDAR, Milano, pp. 97e108. 

Bergada, M.M., Cebria, A., Mestres, J., 2005a. Practicas de estabulacion durante el 

Neolítico antiguo en Catalu~na a traves de la micromorfología: cueva de la 

Guineu (Font-Rubí, Alt Penedes, Barcelona). In: III Congr. del Neolítico la 

Península Iberica, Santander, pp. 187e196. 

Bergada, M.M., Guerrero, V.M., Ensenyat, J., 2005b. Primeras evidencias de 

estabulacion en el yacimiento de Son Matge (Serra de Tramuntana, Mallorca) a 

traves del registro sedimentario. Mayurqa 30, 153e180. 

Bergada, M. M., Cervello, J.M., Edo, M., Antolín, F., Martínez, P., in press. Procesos 

deposicionales y antropicos en el registro holoceno de la Cova de Can Sadurní 

(Begues, Barcelona, Espa~na): aportaciones microestratigraficas. Geoarqueología, 

entre las Ciencias de la Tierra y la Hist./Geoarchaeology, between Earth Sci. Hist. 

Bol. Geol. Minero (2018, 129 (1e2) (Accepted). 

Berger, J.F., 2011. Hydrological and post-depositional impacts on the distribution of 

Holocene archaeological sites: the case of the Holocene middle Rhône River 

basin, France. Geomorphology 129, 167e182. 

Berger, J.F., Guilaine, J., 2009. The 8200 cal BP abrupt environmental change and the 

Neolithic transition: a Mediterranean perspective. Quat. Int. 200 (1), 31e49. 

Berger, J.F., Delhon, C., Magnin, F., Bonte, S., Peyric, D., Thiebault, T., Guilbert, R., 

Beeching, A., 2016. A fluvial record of the mid-Holocene rapid climatic changes 

in the middle Rhone valley (Espeluche-Lalo, France) and of their impact on Late 

Mesolithic and Early Neolithic societies. Quat. Sci. Rev. 136, 66e84. 

Bertran, P., Coutard, J.P., 2004. Solifluxion. In: Bertran, P. (Ed.), Depôt de pente 

continentaux dynamique et facies, vol. 1. Quaternaire, pp. 80e109. 

Bertran, P., Texier, J.P., 1999. Facies and microfacies of slope deposits. Catena 35, 

99e121. 

Blasco, A., Edo, M., Villalba, M.J., 2005a. Cardial, Epicardial y Postcardial en Can 

Sadurní (Begues, Baix Llobregat). El largo fin del Neolítico antiguo en Catalu~na. 

In: III Congreso del Neolítico en la península Iberica. Santander, pp. 867e876. 

Blasco, A., Edo, M., Villalba, M.J., 2005b. Primeros datos sobre la utilizacion sepulcral 

de la cueva de Can Sadurní (Begues, Baix Llobregat) en el Neolítico Cardial. In: 

III Congreso del Neolítico en la península Iberica. Santander, pp. 625e633. 

Bond, G., Showers, W., Cheseby, M., Lotti, R., Almasi, P., Demenocal, P., Priore, P., 

Cullen, H., Hajdas, I., Bonani, G., 1997. A pervasive millenial-scale cycle in North 

Atlantic Holocene and glacial climates. Science 278, 1257e1266. 

Bond, G., Kromer, B., Beer, J., Muscheler, R., Evans, M.N., Showers, W., Hoffmann, S., 

Lotti-Bond, R., Hajdas, I. y, Bonani, G., 2001. Persistent solar influence on North 

Atlantic climate during the Holocene. Science 294, 2130e2136. 

Boschian, G., 2006. Geoarchaeology of pupicina cave. In: Miracle, P.T., Forenbaher, S. 

(Eds.), Prehistoric Herders in Istria (Croatia): the Archaeology of Pupicina Cave 

(1). Archaeological Museum of Istria, Pula. 

Boschian, G., Miracle, P.T., 2007. Shepherds and caves in the karst of Istria (Croatia). 

Atti Soc. Tosc. Sci. Nat. Mem. Ser. A 112, 173e180. 

Brochier, J.E., 1996. Feullies ou fumiers? Observations sur le rôle des opusieres 

spherolitiques dans l'interpretation des depôts archeologiques holocenes. 

Anthropozoologica 24, 19e30. 

Brochier, J.E., 2002. Les sediments anthropiques: methodes d’etude et perspectives. 

In: Miskovsky, J.C. (Ed.), Geologie de la Prehistoire: methodes, techniques, applications, 

second ed. Geopre, Paris, pp. 453e477. 

Bullock, P., Fedoroff, N., Jongerius, A., Stoops, G., Tursina, T., 1985. Handbook for Soil 

Thin Section Description. Waine research publ., Wolverhampton. 

Burjachs, F., Samantha, E.J., Giralt, S.J., Fernandez-Lopez de Pablo, J., 2016. Lateglacial 

to Early Holocene recursive aridity events in the SE Mediterranean Iberian 

Peninsula: the Salines playa lake case study. Quat. Int. 403, 187e200. 

Cacho, I., Grimalt, J.O., Canals, M., Sbaffi, L., Shackleton, N.J., Sch€onfeld, J., Zahn, R., 

2001. Variability of the western Mediterranean Sea surface temperature during 

the last 25,000 years and its connection with the Northern Hemisphere climatic 

changes. Paleoceanography 16/1, 40e52. 

Cacho, I., Valero-Garces, B., Gonzalez-Samperiz, P., 2010. Revision de las reconstrucciones 

paleoclimaticas en la Península Iberica desde el último periodo 

glacial. In: Perez, F.F., Boscolo, R. (Eds.), Clima en Espa~na: pasado, presente y 

futuro. Informe de evaluacion del cambio climatico regional, pp. 9e24. 

Canti, M.G., 1997. An investigation of microscopic calcareous spherulites from 

herbivore dungs. J. Archaeol. Sci. 24, 219e231. 

Canti, M.G., 2003. Aspects of the chemical and microscopic characteristics of plant 

ashes found in archaeological soils. Catena 54, 339e361. 

Carrion, J.S., Fernandez, S., Gonzalez-Samperiz, P., Gil-Romera, G., Badal, E., Carrion- 

Marco, Y., Lopez-Merino, L., Lopez-Saez, J.A., Fierro, E., Burjachs, F., 2010. Expected 

trends and surprises in the lateglacial and Holocene vegetation history 

of the iberian peninsula and balearic Islands. Rev. Palaeobot. Palynology 162 (3), 

458e475. 

Cacho, C., Jorda, J.F., 2009. El Tossal de la Roca: the Pleistocene-Holocene Transition 

in the Mediterranean Region of Eastern Spain. J. Anthropol. Res. 65 (2), 

221e236. 

Combourieu-Nebout, N., Peyron, O., Bout-Roumazeilles, V., Goring, S., Dormoy, I., 

Joannin, S., Sadori, L., Siani, G., Magny, M., 2013. Holocene vegetation and 

climate changes in the central Mediterranean inferred from a high-resolution 

marine pollen record (Adriatic Sea). Clim. Past. 9 (5), 2023e2042. 

Cortes Sanchez, M., Jimenez Espejo, F.J., Simon Vallejo, M.D., Gibaja Bao, J.F., 

Carvalho, A.F., Martinez-Ruiz, F., Rodrigo Gamiz, M., Flores, J.-A., Paytan, A., 

Lopez Saez, J.A., Pe~na-Chocarro, L., Carrion, J.S., Morales Mu~niz, A., Rosello 

Izquierdo, E., Riquelme Cantal, J.A., Dean, R.M., Salgueiro, E., Martínez 

Sanchez, R.M., De la Rubia de Gracia, J.J., Lozano Francisco, M.C., Vera Pelaez, J.L., 

Rodríguez, L.L., Bicho, N.F., 2012. The mesolithiceneolithic transition in southern 

Iberia. Quat. Res. 77 (2), 221e234. 

Courty, M.A., Goldberg, P., Macphail, R.I., 1989. Soils and Micromorphology in 

Archaeology. Cambridge University Press. 

Courty, M.A., Macphail, R.I., Wattez, J., 1991. Soil micromorphological indicators of 

pastoralism; with special reference to Arene Candide, Finale Ligure, Italy. Riv. 

Studiiguri, LVII 1e4, 127e150. 

Davis, B.A., Brewer, S., Stevenson, A.C., Guiot, J., 2003. The temperature of Europe 

during the Holocene reconstructed from pollen data. Quat. Sci. Rev. 22, 

1701e1716. 

Dorronsoro, B., Aguilar, J., Dorronsoro-Díaz, C., Stoops, G., Sierra, M., Fernandez, J., 

Dorronsoro-Fdez, C., 2015. HydroSols. Hidromorfía en suelos. http://www. 

edafologia.net/hidro/index.htm (02/05/2017). 

Durand, N., Curtis, H., Canti, M.G., 2010. Calcium carbonate features. In: Stoops, G., 

Marcelino, V., Mees, F. (Eds.), Interpretation of Micromorphological Features of 

Soils and Regoliths. Elsevier, Amsterdam, pp. 149e194. 

Edo, M., Blasco, A., Villalba, M.J., 2011. La cova de Can Sadurní, guio sintetic de la 

prehistoria recent de Garraf. In: Blasco, A., Edo, M., Villalba, M.J. (Eds.), La Cova 

de Can Sadurní i la prehistoria de Garraf. Recull de 30 anys d’investigacions. 

EDAR, Milano, pp. 13e95. 

Edo, M., Antolín, F., Martínez, P., Castellana, C., Bardera, R., Sa~na, M., Bergada, M. M., 

Fullola, J. M., Barrio, C., Fierro, E., Castillo, T., Fornell, E., in press a. Cueva de Can 

Sadurní (Begues, Barcelona). Hacia la definicion del modelo funerario en cueva 

para el Neolítico Medio I del nordeste peninsular. In: Gibaja, J.F., Subira, M.E., 

Martín, A., Mozota, M., Roig, J. Mirando a la Muerte. Las practicas funerarias 

durante el neolítico en el noreste peninsular. E-ditArx - Publicaciones Digitales, 

Castellon. 

Edo M., Antolín, F., Martínez, P., Villalba, M.J., Fullola, J.M., Bergada, M.M., Sa~na, M., 

Verdún, E., Fernandez-Domínguez, E., Gamba, C., Arroyo-Pardo, E., Ache, M., 

Gibaja, J.F., Palomo, A., Clop, X., Manen, C., in press b. El episodio funerario del 

neolítico antiguo cardial pleno de la cueva de Can Sadurní (Begues, Barcelona). 

Estado actual de la cuestion. In: Gibaja, J.F., Subira, M.E., Martín, A., Mozota, M., 

Roig, J. Mirando a la Muerte. Las practicas funerarias durante el neolítico en el 

noreste peninsular. E-ditArx - Publicaciones Digitales, Castellon. 

Egüez, N., Mallol, C., Martín-Socas, D., Camalich, M.D., 2016. Radiometric dates and 

micromorphological evidence for synchronous domestic activity and sheep 

penning in a Neolithic cave: cueva de El Toro (Malaga, Antequera, Spain). 

Archaeol. Anthropol. Sci. 8 (1), 107e123. 

Equip Guineu, 1995. Elaboracio d’una cronoestratigrafia per a la prehistoria del 

Penedes. Trib. d’Arqueologia 1993e1994, 7e24. 

Fernandez, J., Jochim, M.A., 2010. The impact of the 8,200 cal BP climatic event on 

human mobility strategies during the Iberian late Mesolithic. J. Anthropol. Res. 

66, 39e68. 

Fernandez, F., Dorronsoro-Fdez, C., Aguilar, J., Dorronsoro, B., Stoops, G., Dorronsoro 

Díaz, C., 2015. IlluviaSols. El proceso de iluviacion de arcilla en los suelos (02/05/ 

2017). http://www.edafologia.net/iluv/index.htm. 

Ferrer, C., 2015. Estudios geoarqueologicos en las comarcas meridinales valencianas. 

Procesos sedimentarios holocenos. PhD Thesis. Universitat de Valencia (Unpublished). 

417 pp. http://roderic.uv.es/handle/10550/49367. 

Fitzpatrick, E.A., 1990. Micromorfología de suelos. Compa~nía editorial continental, 

Mexico. 

Fletcher, W.J., Zielhofer, C., 2013. Fragility of Western Mediterranean landscapes 

during Holocene rapid climate changes. Catena 103, 16e29. 

Frigola, J., Moreno, A., Cacho, I., Canals, M., Sierro, J.F., Flores, J.A., Grimalt, J.O., 

Hodell, D.A., Curtis, J.H., 2007. Holocene climate variability in the western 

Mediterranean region from a deepwater sediment record. Paleoceanography 

22, PA2209. https://doi.org/10.1029/2006PA001307, 2007. 

Fullola, J.M., García-Argüelles, P., Mangado, X., Medina, B., 2011. Paleolític i epipaleolític 

al Garraf-Ordal. On erem i on som. In: Blasco, A., Edo, M., Villalba, M.J. 

(Eds.), La Cova de Can Sadurní i la prehistoria de Garraf. Recull de 30 anys 

d’investigacions. EDAR, Milano, pp. 227e243. 

Fumanal, M.P., 1995. Los depositos cuaternarios en cuevas y abrigos. Implicaciones 

sedimentoclimaticas. El Cuaternario del País Valenciano. Universitat de. 

Valencia, Valencia, pp. 115e124. 

García-Argüelles, P., Fullola, J.M., Roman, D., Nadal, J., Bergada, M.M., 2013. El 

modelo epipaleolítico geometrico tipo Filador 40 a~nos despues: vigencia y 

nuevas propuestas Estudios en Homenaje a Javier Fortea Perez. Universitatis 

Ovetensis Magister. Mensula. Editorial: Servicio de publicaciones de la Universidad 

de Oviedo, Oviedo, pp. 151e165. 

García-Puchol, O., Aura, J.E., 2006. El Abric de la Falguera (Alcoi, Alacant). 8000 a~nos 

de ocupacion humana en la cabecera del río Alcoi. Diputacion de Alicante. 

Ayuntamiento de Alcoi y Caja de Ahorros Mediterraneo, Alcoi. 

García-Ruiz, J.M., Palacios, D., Gonzalez-Samperiz, P., Andres, de N., Moreno, A., 

Valero-garces, B., Gomez-Villar, A., 2016. Mountain glaciar evolution in the 





iberian peninsula during the younger Dryas. Quat. Sci. Rev. 138, 16e30. 

Gonzalez-Samperiz, P., Valero-Garces, B.L., Moreno, A., Jalut, G., García-Ruiz, J.M., 

Martí-Bono, C., Delgado-Huertas, A., Navas, A., Otto, T., Dedoubat, J.L., 2006. 

Climate variability in the Spanish Pyrenees during the last 30,000 yr revealed 

by the Portalet sequence. Quat. Res. 66 (1), 38e52. 

Gonzalez-Samperiz, P., Utrilla, P., Mazo, C., Valero-Garces, B., Sopena, M.C., 

Morellon, M., Sebastian, M., Moreno, A., Martínez-Bea, M., 2009. Patterns of 

human occupation during the early Holocene in the Central Ebro Basin (NE 

Spain) in response to the 8.2 ka climatic event. Quat. Res. 71 (2), 121e132. 

Jalut, G., Esteban Amat, A., Bonnet, L., Gauquelin, T., Fontugne, M., 2000. Holocene 

climatic changes in the Western Mediterranean, from south-east France to 

south-east Spain. Palaeogeogr. Palaeoclimatol. Palaeoecol. 160 (3), 255e290. 

Jalut, G., Dedoubat, J.J., Fontugne, M., Otto, T., 2009. Holocene circum- 

Mediterranean vegetation changes: climate forcing and human impact. Quat. 

Int. 200 (1), 4e18. 

Jorda, J.F., Mora, R., Pique, R., 1992. La secuencia litoestratigrafica y arqueologica del 

yacimineto de la Font del Ros (Berga, Barcelona). Cuaternario Geomorfol. 6, 

21e30. 

Karkanas, P., Goldberg, P., 2010. Phosphatic features. In: Stoops, G., Marcelino, V., 

Mees, F. (Eds.), Interpretation of Micromorphological Features of Soils and 

Regoliths. Elsevier, Amsterdam, pp. 521e541. 

Karkanas, P., Goldberg, P., 2013. Micromorphology of cave sediments. In: 

Shroder, John F., Frumkin, A. (Eds.), Treatise on Geomorphology, vol. 6. Karst 

Geomorphology, Academic Press, San Diego, pp. 286e297. 

Lowe, J.J., Rasmussen, S.O., Bj€orck, S., Hoek, W.Z., Steffensen, J.P., Walker, M.J.C., 

Yu, Z.C., 2008. Synchronisation of palaeoenvironmental events in the North 

Atlantic region during the Last Termination: a revised protocol recommended 

by the INTIMATE group. Quat. Sci. Rev. 27, 6e17. 

Macphail, R.I., Courty, M.A., Hather, J., Wattez, J., 1997. The soil micromorphological 

evidence of domestic occupation and stabling activities. Mem. dell’Instituto Ital. 

Paleontol. Um. 53e86. 

Martrat, B., Grimalt, J.O., Shackleton, N.J., de Abreu, L., Hutterli, M.A., Stocker, T.F., 

2007. Four climate cycles of recurring deep and surface water destabilizations 

on the Iberian margin. Science 317 (5837), 502e507. 

Mayewski, P.A., Rohling, E.E., Stager, J.C., Karlen, W., Maasch, K.A., Meeker, L.D., 

Meyerson, E.A., Gasse, F., van Kreveld, S., Holmgren, K., Lee-Thorp, J., 

Rosqvist, G., Rack, F., Staubwasser, M., Schneider, R.R., Steig, E.J., 2004. Holocene 

climate variability. Quat. Res. 62, 243e255. 

McGowan, G., Prangnell, J., 2006. The significance of vivianite in archaeological 

settings. Geoarchaeology An Int. J. 21 (1), 93e111. 

Montes, L., Domingo, R., Gonzalez-Samperiz, P., Sebastian, M., Aranbarri, J., 

Casta~nos, P., García-Simon, L.M., Alcolea, M., Laborda, R., 2016. Landscape, resources 

and people during the Mesolithic and Neolithic times in NE Iberia: the 

Arba de Biel Basin. Quat. Int. 403, 133e150. 

Morales, J.I., Oms, X., 2012. Las últimas evidencias mesolíticas del NE peninsular y el 

vacío pre-neolítico. Rubricatum 5, 35e41. 

Morellon, M., Valero-Garces, B., Vegas-Villarrúbia, T., Gonzalez-Samperiz, P., 

Romero, O., Delgado-Huertas, A., Mata, P., Moreno, A., Rico, M., Corella, J.P., 

2009. Lateglacial and Holocene palaeohydrology in the western Mediteranean 

regio: the lake Estanya record (NE Spain). Quat. Sci. Rev. 28 (25e26), 

2582e2599. 

Moreno, A., Gonzalez-Samperiz, P., Morellon, M., Valero-Garces, B.L., 2012. Northern 

Iberian abrupt climate change dynamics during the last glacial cycle: a view 

from lacustrine sediments. Quat. Sci. Rev. 36, 139e153. 

Moreno, A., Sancho, C., Oliva, B., Bartolome, M., Cacho, I., Stoll, H., Edwards, I.R., 

Cheng, H., Hellstrom, J., 2013. Registro espeleotemico de la variabilidad climatica 

durante el Holoceno: la cueva de Molinos (Teruel). In: Banea, R., 

Fernandez, J.J., Guerrero, y I. (Eds.), El cuaternario iberico: investigacion en el s. 

XXI. Sevilla, pp. 118e122. 

Mücher, H., Van Steijn, H., Kwaad, F., 2010. Colluvial and mass wasting deposits. In: 

Stoops, G., Marcelino, V., Mees, F. (Eds.), Interpretation of Micromorphological 

Features of Soils and Regoliths. Elsevier, Amsterdam, pp. 37e48. 

Nicosia, C., 2008. Micromorphology of some phosphatic inclusions and neoformations 

of ocurring in archaeological deposits. Frankf. Geowiss. Arb. 30, 

85e94. 

Oms, F.X., Mestres, J., Cebria, A., Morales, J.I., Nadal, J., Pedro, M., Mendiela, S., 

Martín, P., Fullola, J.M., 2016. La Cova de la Guineu (Font-Rubí, Barcelona) i les 

relacions plana e muntanya al Penedes durant el Neolític inicial. Tv. SIP 119, 

97e107. 

Perez-Obiol, R., Jalut, G., Julia, R., Pelachs Ma~nosa, A., Iriarte Chiapusso, M.J., Otto, T., 

Hernandez Beloqui, B., 2011. Mid-Holocene vegetation and climatic history of 

the Iberian Peninsula. Holocene 21 (1), 75e93. 

Perez-Sanz, A., Gonzalez-Samperiz, P., Moreno, A., Valero-Garces, B., Gil-Romera, G., 

Rieradevall, M., Tarrats, P., Lasheras- Alvarez, L., Morellon, M., Belmonte, A., 

Sancho, C., Sevilla-Callejo, M., Navase, A., 2013. Holocene climate variability, 

vegetation dynamics and fire regime in the central Pyrenees: the Basa de la 

Mora sequence (NE Spain). Quat. Sci. Rev. 73, 149e169. 

Petit, M.A., Mangado, X., Fullola, J.M., Bartrolí, R., Bergada, M.M., Esteve, X., 2009. Els 

caçadors-recol.lectors de la cova del Parco (Alos de Balaguer, La Noguera, 

Lleida): L'Epipaleolític microlaminar: continuïtat o canvi?. In: Els Pirineus i les 

arees circumdants durant el Tardiglacial. Mutacions i filiacions tecnoculturals, 

evolucion paleoambiental (16.000-10.000 B.P.), XIV Col.loqui Internacional 

d'Arqueologia de Puigcerda. Inst. d'Estudis. Ceretans i Patronat F. Eiximenis, 

Puigcerda, pp. 579e591. 

Polo Díaz, A., 2010. Rediles prehistoricos y uso del espacio en abrigos bajo roca en la 

Cuenca Alta del Ebro: geoarqueología y procesos de formacion durante el 

Holoceno. PhD Thesis. Universidad del País Vasco-Euskal Herriko Unibertsitatea 

(Unpublished). 

Polo Díaz, A., Martínez-Moreno, J., Benito-Calvo, A., Mora, R., 2014. Prehistoric 

herding facilities: site formation and archaeological dynamics in Cova Gran de 

Santa Linya (Southeastern Prepyrenees, Iberia). J. Archaeol. Sci. 41, 784e800. 

Reed, J.M., Stevenson, A.C. y, Juggins, S., 2001. A multi-proxy record of Holocene 

climatic change in Southwestern Spain: the Laguna de Medina, Cadiz. Holocene 

11 (6), 707e719. 

Riera, S., Esteve, X., Nadal, J., 2007. Systemes d’exploitation et anthropisation du 

paysage mediterraneen du Neolithique ancien au premier âge du Fer: le cas de 

la depression de Penedes (nord-est de la peninsule iberique). Environnements 

et cultures a l’âge du Bronze en Europe Occidentale, (Actes des congres nationaux 

des Societes historiques et scientifiques 129e, Besançon, 2004) Editions du 

CTHS, Paris, pp. 121e141. 

Rohling, E.J., P€alike, H., 2005. Centennial-scale climate cooling with a sudden cold 

event around 8,200 years ago. Nature 434 (7036), 975e979. 

Stoops, G., 2003. Guidelines for Analysis and Description of Soil and Regolith Thin 

Section. Soil Science Society of America, Ionc, Wisconsin, Madison. 

Valero-Garces, B.L., Moreno, A., 2011. Iberian lacustrine sediment records: responses 

to past and recent global changes in the Mediterranean region. J. Paleolimnol. 

46, 319e325. 

Vallverdú, J., Carrancho, A., 2004. Estratigrafia del Molí del Salt. In Vaquero, M. Els 

darrers caçadors erecol.lectors de la conca de Barbera: el jaciment del Molí del 

Salt (Vimbodí). Excavacions, pp. 1999e2003. Montblanc, pp.61 e 68. 

Vanniere, B., Power, M.J., Roberts, N., Tinner, W., Carrion, J., Magny, M., Bartlein, P., 

2011. Circum-Mediterranean fire activity and climate changes during the mid 

Holocene environmental transition (8500 e 2500 cal yr BP). Holocene 21 (1), 

53e73. 

Verdasco, C., 2016. Estudio microsedimentologico de niveles arqueosedimentarios 

depositados en cuevas y abrigos en el país valenciano durante el Pleistoceno- 

Holoceno (11.000e5.000 BP). PhD Thesis. Universitat de Valencia (Unpublished). 

http://roderic.uv.es/handle/10550/50641. 

Verges, J.M., Burguet-Coca, A., Allue, E., Exposito, I., Guardiola, M., Martín, P., 

Morales, J.I., Burjachs, F., Cabanes, D., Carrancho, A., Vallverdú, J., 2016. The Mas 

del Pepet experimental programme for the study of prehistoric livestock 

practices: preliminary data from dung burning. Quat. Int. 414, 304e315. 

Van Vliet-Lano€e, B., 2010. Frost action. In: Stoops, G., Marcelino, V., Mees, F. (Eds.), 

Interpretation of Micromorphological Features of Soils and Regoliths. Elsevier, 

Amsterdam, pp. 81e108. 

Wanner, H., Solomina, O., Grosjean, M., Ritz, S.P., Jetel, M., 2011. Structure and origin 

of Holocene cold events. Quat. Sci. Rev. 30, 3109e3123. 

Weninger, B., J€oris, O., Danzeglocke, U., 2007. Glacial Radiocarbon Age Conversion. 

Cologne Radiocarbon Calibration and Palaeoclimate Research Package< CAL- 

PAL> User Manual. Universit€at zu K€oln, Institut für Ur-und Frühgeschichte 

(2009 on line). www.calpal.de/.

Chronostratigraphy in karst records from the Epipaleolithic to the Mid/Early Neolithic (c. 13.0e6.0 cal ka BP) in the Catalan Coastal Ranges of NE Iberia: environmental changes, sedimentary processes and human activity

Create successful ePaper yourself

Delete template?

Save as template?