Quaternary Science Journal - Micromorphology and Site Formation at Hohle Fels Cave, Schwabian J... by Geozon Science Media

Eiszeitalter

und

Gegenwart

1-25 27 A b b . , 2 Tab.

Hannover

2003

Micromorphology and Site Formation at Hohle Fels Cave, Swabian Jura, Germany P A U L GOLDBERG, SOLVEIG SCHIEGL, K A R E N M E L I G N E , C H R I S DAYTON & NICHOLAS J . C O N A R D ^

Keywords: caves, FTIR, micromorphology, Late Quaternary climate, Upper Palaeolithic Abstract: Hohle Fels Cave near Schelklingen in the Swabian Jura area of southwestern Germany, contains an occupational and sedimentological record that spans at least the last 36,000 yeats and includes Aurignacian, Gravettian, and Magdalenian prehistoric occupations. The sediments were subjecred to detailed micromorphological analysis coupled with microanalytical data using electron microprobe and FTIR techniques. The results show that much of the sediment has been de rived from the interior of the cave where the finer ma trix was partially phosphatized, likely derived from bear habitation. Moreover, the sediment has been subjected to cryoturbation and ice lensing under cold and damp conditions. These cold-related features become increas ingly well developed in the Gravettian and Magdale nian layers reflecting more marked cooling during these periods. There is no evidence for the occupation of the cave by humans or cave bears during the Last Glacial Maximum. These geoarchaeological observations can be used test hypotheses about paleoclimate and human behavior developed using independent lines of evidence provided from botanical, faunal and archaeological ma terials. Some of the methods employed in this research have not previously been used to study the caves of the Swabian Jura and provide key new insights into the ar chaeological and natural history of the region. 'Anschrift der Verfasser: P. GOLDBERG, K. M E LIGNE, C. DAYTON: Department of Archaeology, Boston University, 675 Commonwealth Avenue, Boston Massachusetts 0 2 2 1 5 , U.S.A. E-mail: paulberg@bu.edu; N . CONARD, S. SCHIEGL: Institut für Ur- und Frühgeschichte und Archäologie des Mittelalters der Universität Tübingen, Abteilung für Ältere Urgeschichte und Quartärökologie, Schloss Hohentübingen, D-72070 Tübingen

Zusammenfassung: Die Höhle Hohle Fels liegt auf der Schwäbischen Alb bei Schelklingen und beinhaltet eine stratigraphische Folge, die mindestens 36.000 Jahre zurück geht und Aurignacien-, Gravettien- und Magdalenien-Fundschichten beinhaltet. Die Sedimen te vom Hohle Fels wurden mit mikromorphologischen Analysen in Kombination mit Elektronmikroprobe und FTIR-Analysen untersucht. Die Ergebnisse zeigen, dass die Sedimente aus dem inneren Bereich der Höhle stammen und das die feine Matrix in Zusammenhang mit der Nutzung der Höhle durch Bären eine starke Phosphatenanreicherung erlebt hat. Mikrostruktu ren belegen kalte und feuchte klimatische Phasen, chararkterisiert durch Kryoturbation und Eislinsen. Diese Merkmale sind in den Gravettien- und Magdalenien-Schichten stärker entwickelt und sprechen für kühle Bedingungen während dieser Perioden. Während des letzten Kältemaximums fehlen Hinweise für die Nutzung der Höhle durch Menschen und Höhlen bären. Diese Beobachtungen können als Grundlage dienen, um Hypothesen über das Paläoklima und über menschliches Verhalten im Paläolithikum, die anhand botanischer, faunistischer und archäologischer Daten entwickelt wurden, zu prüfen. Einige der Methoden dieser Untersuchungen wurden zum ersten Mal in den Höhlen der Schwäbischen Alb eingesetzt und lieferten viel versprechende Einblicke in die Archäologie und die naturhistorische Enrwicklung der Region.

1 Introduction Paleolithic excavations i n the caves of

the

S w a b i a n J u r a have been c o n d u c t e d s i n c e the 1 8 6 0 s . T h i s rich research tradition i n c l u d i n g the w o r k of Oscar Fraas, R. R. S c h m i d t , G u s tav R i e k a n d others h a s its i n t e l l e c t u a l a n d

PAUL GOLDBERG, SOLVEIG SCHIEGL, KAREN MELIGNE, C H R I S DAYTON & NICHOLAS J . CONARD

methodological

roots

the

2 Site Setting and Stratigraphy

geosciences,

a n d s i n c e its o r i g i n s in t h e e a r l y 2 0 t h C e n tury, the D e p a r t m e n t of E a r l y P r e h i s t o r y a n d

Hohle Fels C a v e is situated on the eastern ex

Q u a t e r n a r y E c o l o g y has h a d s t r o n g l i n k s to

tension of the Swabian Jura about 2 0 k m west

the g e o s c i e n c e s of the U n i v e r s i t y of T ü b i n

of U l m (Figures 1 and 2 ) . T h e cave is formed

gen. D e s p i t e t h e long a n d successful research

within an U p p e r Jurassic ( M a l m ) limestone reef

tradition

a n d occurs at about 5 3 4 m above sea level (asi)

geoarchaeology work

Tübingen,

which

i n c l u d e s recent

by J .

Hahn,

(HAHN

1 9 8 8 ) , H . LAVII.EE (LAVII.EE &

in the valley of the Ach River, a tributary of the

HAHN

Danube. T h e A c h Valley was cut by the D a n u b e

1 9 8 1 ) a n d I. C A M P E N ( 1 9 8 7 ) , it w a s not u n t i l

before it left its bed shortly d u r i n g the Riss g l a

the l a t e 1 9 9 0 s t h a t c o n t e m p o r a r y

cial m a x i m u m (VIELINGER 1 9 8 6 ) . Today the A c h

including

micromorphological

methods

studies

and

Rivet is about 3 m wide a n d flows to the east

m i c r o a n a l y t i c a l t e c h n i q u e s , s u c h as e l e c t r o n

into the blau river. Prior to the Riss Glacial Peri

m i c r o p r o b e a n d F T I R h a v e b e e n a p p l i e d to

od the valley b o t t o m was up to 4 0 m lower than

answer archaeological and paleoenvironmen-

today a n d m u c h narrower; it has subsequently

tal q u e s t i o n s r e l a t e d to t h e P a l e o l i t h i c cave

been filled w i t h gravel a n d sand. T h e cave is

e x c a v a t i o n s in the S w a b i a n J u r a . W i t h this

located on the southeast side of the valley, a b o u t

paper w e p r e s e n t a series of results u s i n g n e w

7 m above the current valley b o t t o m w h i c h here

m e t h o d s to a d d r e s s research q u e s t i o n s range from site f o r m a t i o n to

that

is about 3 5 0 m w i d e . During the terminal Pleis

environmental

tocene the valley bottom was ca. 5 - 1 0 m lower

c h a n g e , from t h e c u r r e n t e x c a v a t i o n s at H o h

than today's position (WAGNER 1 9 7 9 ) .

le Fels n e a r S c h e l k l i n g e n in t h e A c h V a l l e y of

Hohle Fels is one of the largest caves in the re-

southwestern

Germany.

Fig. 1: Location Map of Hohle Fels Cave in the Swabian Jura.

Micromorphology and Site Formation at Hohle Fels Cave, Swabian Jura, Germany

gion with a large cave hall that has a m a x i m u m 2

height of 12 m a n d covers a n area of 500 m .

Wattle

T h e entrance is connected w i t h the cave hall

HB__gh. '«*_ B__M_f

by a 3 0 m long passage (Figure 3 ) . During t h e

first

scientific excavations i n 1 8 7 0 / 7 1

Oscar

Fraas recovered a n enormous n u m b e r of cave bear bones, as well as stone, bone, and antler artifacts. R . R . S c h m i d t (SCHMIDT 1910, 1 9 1 2 ) presented the Paleolithic from H o h l e Fels in h i s classic m o n o g r a p h , „Die d i l u v i a l e Vorzeit Deutschlands". From

1 9 5 8 - 1 9 6 0 G. Matschak a n d

G. Riek c o n d u c t e d excavations i n several parts of the cave, most notably i n a large niche o n

the left side of t h e passage l e a d i n g to the m a i n

_ _ _ _ _ _ _ t .

HHP-.

hall of the cave. T h e excavators never published

i£HL* H ^ H R s -

their results, a n d C . Saier (SAIER 1994) was t h e first to systematically study t h e finds from these

IlliP ^^!

excavations. Between 1 9 7 7 - 7 9 a n d 1 9 8 7 - 1 9 9 6 Joachim H a h n renewed excavations in the niche in the hopes o f g a i n i n g a stratigraphic section for comparison w i t h the profile from

nearby

•

Geißenklösterle (HAHN 1 9 8 8 ) . Archaeological, palaeontological a n d geological research results

from Hohle Fels have been p u b l i s h e d in numerous articles a n d

theses (BI.UMENTRITT & H A H N

1991;

FISCHER et al. 1 9 9 3 ; H A H N 1989a, 1 9 8 9 b ,

1991,

1992, 1 9 9 5 ; HAHN & PASDA 1990; OBER-

MAIER 1 9 0 6 ; R A H L E 1 9 8 1 ; SCHEER

Hahn's death i n 1997,

1994). Since

N . C o n a r d and H . P.

U e r p m a n n have directed t h e ongoing excavations (CONARD & UERPMANN

1 9 9 9 ; CONARD &

FLOSS 1 9 9 9 , 2 0 0 0 ; CONARD et al. 2 0 0 0 , 2 0 0 2 ) . T h i s latest w o r k has revealed a sequence of

ebou-

/w-rich silty a n d clayey deposits, some rich i n charcoal and b u r n t bone. In addition, a n u m b e r of

archaeological

that range from

horizons

were

recognized

A u r i g n a c i a n strata at the base

through Gravettian a n d M a g d a l e n i a n layers at

Fig. 2: Hohle Fels Cave entrance. on parameters such as color, texture, a n d internal organization. These are described in Table 1. T h e archaeological

horizons

( A H ) or Units, on

the other h a n d , are determined on the basis of the assemblages of artifactual material. In the case of H o h l e Fels, lithological a n d archaeological b o u n d a r i e s are strongly linked. At a more general level of analysis four m a i n stratigraphic units ( A - D ) have been defined for operational reasons ( C O N A R D & UERPMANN

1 9 9 9 ; Table 1 ) .

Each of these units is discussed from b o t t o m to top as follows: Unit

the top (Figures 3 , 4; Table 1 ) .

ilBHHi

D (the Aurignacian) - Unit D was uncov2

ered over a n area of 6 m (CONARD et al. 2 0 0 2 ) , a n d so far, consists of well stratified geological T h e stratigraphic sequence at H o h l e Fels can be

layers 3 d - 8 a n d archaeological horizons A H I l d -

considered from the standpoints of both litho-

V. A l t h o u g h w e have not yet reached the b o t t o m

and archaeo-stratigraphy. T h e former approach

of this unit, thus far, about 1 m of s e d i m e n t s

results in several geological

( G H ) or

has been excavated (see CONARD et a l . 2 0 0 2 ) .

Layers that follow standard field criteria based

T h e majority o f lithic artifacts was produced o n

horizons

PAUL GOLDBERG, SOLVEIG SCHIEGL, KAREN MELIGNE, C H R I S DAYTON & NICHOLAS J . CONARD

Fig. 3: Profile 2 showing stratigraphy with archaeological units and geological layers, as well as sampling locations. The inset map shows the deep interior chamber and the location of excavated area with exposures of sediments discussed in the text. The grid lines are 1 m apart. local cherts. U n l i k e overlying Gravettian assem

recognizable strata. T h e m a i n occupation of the

blages, i m p l e m e n t s m a d e on radiolarite are con

Gravettian complex dates to ca. 2 9 , 0 0 0 - 2 7 , 0 0 0

siderably less abundant.

years BP.

L a c k of debitage a n d

cores suggests the absence of in situ k n a p p i n g

M o r e than

scatters, but discarded stone tools are c o m m o n

unmodified debitage. Cores a n d tools are also

and include diverse forms typical for the Swa

numerous,

bian A u r i g n a c i a n . I m p l e m e n t s and

Gravette points, and end scrapers (CONARD et

ornaments

9 0 % of the lithic assemblage is including

backed

knifes,

burins,

produced from ivory as well as ivory w o r k i n g

al. 2 0 0 0 ) .

debris are c o m m o n , a n d three m a m m o t h ivory

to those of the M a g d a l e n i a n tools (BURKERT &

figurines have been recovered from the A u r i g n a

FLOSS in press). A rich inventory of bone, antler

cian layers from Hohle Fels. T h e faunal analysis

and ivory tools as well as antler picks a n d per

is still underway, but p r e l i m i n a r y analysis has

forated batons have been recovered (CONARD &

documented

bear,

FLOSS 2 0 0 1 ) . T h e Gravettian archaeological ho

horse, reindeer, fox, a n d hare. Furthermore, a

rizons have yielded n u m e r o u s pendants of ivory

the presence of m a m m o t h ,

T h e lithic raw materials are s i m i l a r

well-defined concentration of burnt bone w a s

and perforated teeth.

unearthed

T h e faunal record of the Gravettian layers has

in the lower Aurignacian

horizon

IV. A series of radiocarbon dates for these Au

not

rignacian layers have y i e l d e d uncalibrated ages

show that cave bears are well represented, a n d

been

fully

analyzed. Preliminary

results

between 3 0 a n d 3 6 ka. T h e s e dates are consist

in 2 0 0 0 a vertebra of a cave bear was recovered

ent w i t h the relatively early dates for the Aurig

from A H Ilcf with an e m b e d d e d fragment

nacian at nearby sites i n c l u d i n g Geißenklösterle

a chert w e a p o n . This

(CONARD & BOLES in press). Geological samples

conclusive evidence for active h u n t i n g of cave

from U n i t D have not yet been studied.

bear.

find

provides the

of first

Nonetheless, the w e i g h t of evidence sug

Unit C (the Gravettian) - T h e Gravettian lay

gests that the majority of cave bear bone resulted

ers 3b - 3cf (AH Ilb-IIcf), are 6 0 - 8 0 c m thick,

from natural mortality (MUNZEL et al. 2 0 0 1 ) .

and have been uncovered over an area of ca 3 0

Horse appears to be the m a i n g a m e species, a n d

m . T h e sediments of these layers are well pre

reindeer is present but less a b u n d a n t . As in the

served, a n d m a n y finds of these layers are from

A u r i g n a c i a n and M a g d a l e n i a n deposits,

much

Micromorphology and Site Formation at Hohle Fels Cave, Swabian Jura, Germany

Tab. 1: Sediment and profile description of Hohle Fels Cave (Schelklingen, Southern Germany)

Profile 2 (cf. Fig. 4) Geol. Horizon/ UNITS

Field o b s e r v a t i o n s

Munsell Color

Arch. Horizon/ LAYERS

Archaeological features and Comments

1 4

Uncalibrated C Age (AMS in italics)

1. Modern Stratigraphic Complex a

2.5Y 7/4

5 Y 2.5/1

7.5YR 3/4

2.5Y 5/6

0 Cave pavement (Höhlenfestschichten) consisting of alternating banded layers up to 2 cm in diameter; coarse yellow, rectangular gravel and blackish fine sedimentbearing pebbles. 0 Slag-bearing layer containing pebble chips and few 34cm size pebbles mixed with some finer clayey sediment Thin gravel "leveling layer" with rounded pebbles up to 0 2cm across. Sandy sediment containing limestone gravel with boulders up to 45 cm in diameter. Gravel displays preferred sub-horizontal orientation. Yellow - ochre.

Post-1958

1944 1944

2. S t r a t i g r a p h i c A - c o m p l e x ( H o l o c e n e ; b e l o w Unit 1 k, p u r e a n d t y p i c a l M a g d a l e n i a n Oc

5Y 2.5/1

Maqdalenian 1k 2.5Y 2/0

Slightly rounded to well rounded 2-5 c m size limestone fragments lacking preferred orientation. They occur within a dark grey/black argillaceous silt with fine grained calcareous sand.

0/1

Mixed horizon: containing metal age and Neolithic ceramics and Magdalenian artefacts; disturbed Holocene surface caused by clearing in 1944

Clayey silt with 1-2 mm size irregularly to slightly rounded limestone gravel, slightly elongated and without recognizable orientation.

Magdalenian lithic 13,240 ±110 and organic 13,085 ± 95 artifacts 12,770 ± 2 2 0

Contains black fired ceramics

Pit filling of Q u 7 6 / 7 7 / 8 6 / 8 7 1gb

10YR 5/2

Medium grey, very dense clay, with homogeneous distribution of rather big-charcoal fragments. Inclusions of medium sized, angular to slightly rounded limestone.

Stratigraphic B-Complex (moonmilk-sediments and limestone gravel) 1s

10YR 8/2

3as

2.5Y 5/6

White, fine calcific sand with slight amount of interstitial clayey silt; subangular limestone inclusions, 2-5 cm, mostly without orientation. Very heterogeneous layer. In the northern part, a marked unconformity separates a matrix-rich area from a matrix-poor one. Matrix-rich area: Matrix is pale yellow/brown, pale grey/brown, partly darker brown silty with little clay and fine sand. High abundance of 1-8 c m , angular limestone gravel inclusions displaying irregular orientation, occurring along with very well rounded, 1cm diameter clasts. Matrix-poor area: Matrix is virtually lacking, and clasts consist mostly of 2-8 cm, and some 10-13 cm of limestone fragments/gravel; these are angular to rounded, and irregular to slightly elongated shape, without orientation.

essentially sterile

PAUL GOLDBERG, SOLVEIG SCHIEGL, KAREN MELIGNE, C H R I S DAYTON & NICHOLAS J . CONARD

Stratiqraphic C-Complex (mainly Gravettian) 3ad 10YR3/2-4/4 Heterogeneous layer with pockets of variable brightness I/I I b (generated by washing out of finer components) containing sedimentologically different types of infillings; the darker sediment infillings possibly exhibit an anthropogenic component. The lighter matrix consists of dark grey-brown silt with small amounts of clay and calcareous sand. The dark matrix is blackish silt with small amounts of calcareous sand and a somewhat higher clay component compared to areas of the bright matrix. Inclusions (2-7 cm) are relatively abundant, mostly angular, but some partly rounded; they dip northwards. 3bcomplex

7.5YR4/6

3bt

2.5Y2/3

10YR5/6

3cf

5Y 2.5/1

Reddish silt with little clay and fine calcareous sand. Inclusions of angular to slightly rounded limestone gravel occur in variable amounts without orientation. Dark grey, partly black silt, with an abundance of sand size burnt bone (Knochenkohle) and a small amount of clay. Inclusions consist of some stones, bones and bone ash (>1cm). Very moist clayey silt with many limestone clasts of variable sizes. They are angular to rounded, and dip towards the NE. Black clayey silt with a high proportion of bone ash that underlies a limestone-rich gravel layer.

Mixed Magdalenian/Gra vettian-horizon (reworked and displaced Gravettian)

Gravettian lithic and organic artifacts Gravettian lithic and organic artifacts

27,150 ± 600

Gravettian lithic and organic artifacts Gravettian lithic and organic artifacts

29,550 ± 650

II d

Aurignacian ?

29,560 + 240/-230 30,010 ± 2 2 0

II e

Aurignacian lithic and organic artifacts Aurignacian lithic and organic artifacts

II b

II c

28,920

±400

Stratigraphic D-Complex (mainly Aurignacian) 3d

10YR 4/4

7.5YR 4/4

7.5YR 5/6

Red-brown argillaceous silt with ca. 6 0 % of 4 - 8 c m , slightly rounded limestone gravel inclusions. Matrix only slightly compacted, contains abundant small pores and cavities. Generally loose mixture of angular limestone gravel and moist clayey silt with a minor component of coarse calcareous sand. Rounded limestone gravel with little interstitial matrix. Mostly coarse-grained calcareous sand, downwardfacing edges or fracture planes of limestone fragments frequently bear grey clay crusts.

III

30,550 ± 5 5 0 31,100 ±600

Notes o n d e s c r i p t i o n s : 1} These are provisional descriptions based on unpublished work by J. Hahn (12.09.1994); Waiblinger (1997); N.J. Conard and T. Prindiville (02.09.1997); and P. Russell and N.J. Conard (09.98). The geological and archaeological horizons (GH and AH) serve as preliminary field descriptions and are subject to modification during future excavations. 2) Colors were determined using the Munsell Soil Color Chart on moist samples, both in the cave under artificial light conditions and outside the cave in natural light. 3) Differentiation of individual sediment units on the basis of their calcium carbonate contents was not possible due to the large number of limestone clasts. 4)

C ages are uncalibrated and compiled from Conard and Bolus (2003); Conard and Floss (2000); Hofreiter et al. (2002); and Housley et al. (1997).

of a r c h a e o f a u n a has been systematically b u r n t

reach a m a x i m u m thickness a r o u n d 7 0 c m next

for fuel. F r a g m e n t s of bone of large g a m e , such

to the wall of the cave in the northern p a r t of

as m a m m o t h a n d rhinoceros are also present.

the excavation (Figure 4 ) ; these deposits t h i n

Large, m e d i u m a n d small g a m e , such as fox

out toward the interior of the niche.

and ha r e p l a y e d a p r o m i n e n t part of the h u m a n

trast to the other strata, the horizons of u n i t B

e c o n o m y — i n c l u d i n g use of hides, raw material

are light colored.

and food.

proportions

In c o n

T h i s feature is due to h i g h

of rubble- a n d sand-sized l i m e

stone, a n d l o w a m o u n t s of clay, especially in the Unit B (archaeologically sterile) — Unit B con

upper horizon. T h e B - c o m p l e x is a r c h a e o l o g i

sists of t w o layers ( I s a n d 3 a s ) , w h i c h together

cally nearly sterile a n d lacks datable m a t e r i a l .

Micromorphology and Site Formation at Hohle Fels Cave, Swabian Jura, Germany 3 Laboratory Methods

T h e rare artifacts recovered from this c o m p l e x are a p p a r e n t l y not in situ

a n d were likely i n

corporated i n t o the s e d i m e n t b y cryoturbation.

S a m p l e s a n d sample p r e p a r a t i o n

Consistent w i t h its sterile n a t u r e , its s e d i m e n t o -

Cave sediments are typically c o m p l e x mixtures

logical c o m p o s i t i o n , a n d t h e radiocarbon d a t e s

of cultural a n d geological materials that are

from the over- a n d u n d e r l y i n g deposits, t h e

c o m m o n l y diagenetically altered (WEENER et a l .

B-complex c a n be reasonably correlated w i t h

1995).

W e thus chose a m i c r o m o r p h o l o g i c a l

the Last G l a c i a l M a x i m u m . N o clear evidence

approach that includes the s t u d y of u n d i s t u r b e d

of occupation has been discovered so far in t h e

samples b y light microscopy c o u p l e d w i t h S E M

Swabian J u r a d u r i n g this interval.

study a n d elemental analysis of the in tact sedi ments.

Unit A ( t h e M a g d a l e n i a n ) - T h e M a g d a l e n i a n complex has been excavated over an area of 3 0

A set of thirteen large samples of u n d i s t u r b e d blocks of sediment w a s collected a l o n g the

a n d has a thickness of 2 0 - 6 0 cm. M u c h o f

western profile of the excavated entrance section

the sediments has been modified by cryotur

(Figures 3 a n d 4 ) . A n a d d i t i o n a l s a m p l e (no.

bation i n h i b i t i n g the establishment of a fine

14) was taken in excavation square 7 7 , about 1

stratigraphy

m a w a y from the profile.

T h e cave s e d i m e n t s

upper layers also contain diverse finds from

characteristically

major

the H o l o c e n e , such as pottery,

demonstrating

limestone gravel - m m to several d m i n size

that considerable m i x i n g h a s occurred. T h e

- derived from the roof a n d walls of the cave.

M a g d a l e n i a n complex dates to ca. 13,000 y e a r s

S a m p l i n g such stony deposits is difficult, a n d it

BP.

was not possible to use K u b i e n a boxes.

(CONARD

FLOSS

2001).

The

contain

amounts

Instead,

the M a g d a l e n i a n

we jacketed large areas of s e d i m e n t exposed in

deposits i n c l u d e mostly b l a d e s and bladelets,

Profile 2 w i t h burlap d i p p e d i n plaster of Paris.

although scrapers, burins, borer, backed k n i v e s

After the exposed part of t h e plaster jackets

and backed points have also been uncovered.

hardened, the block was carefully removed from

T h e y are p r o d u c e d m a i n l y from local Jurassic

the profile a n d the rear p o r t i o n w a s s i m i l a r l y

chert a n d radiolarite, a l t h o u g h non-local r a w

covered w i t h plaster-impregnated burlap.

materials a r e also present (BURKERT & FLOSS i n

In the laboratory several 1-2 c m large w i n d o w s

press).

were c u t through the plaster prior to 6 weeks

N u m e r o u s b o n e a n d antler tools, such as p r o

of d r y i n g at 60° C in a d r y i n g oven. After d r y

jectile points, o n e d o u b l e - r o w e d harpoon a n d

ing, the blocks were put into large containers

several needles also occur.

and partly covered with a m i x t u r e of styrene-

The

lithic

artifacts

from

T h e Magdalenian

assemblage contains w o r k e d pieces of jet a n d

based polymeric resin (Viscovoss N 5 0 S b y

ivory, as w e l l as perforated snail shells and teeth.

Voss C h e m i e G m b H ) , styrene ( M e r c k Eurolab

In 1998 excavations recovered a painted r o c k

GmbH)

fragment, w h i c h might h a v e been a p a i n t e d

C h e m i e G m b H ) in relative v o l u m e proportions

piece of t h e cave wall, or alternatively, c o u l d

7:3:

a n d hardener

(MEKP

M E C , Voss

0 . 0 2 5 . T h e containers kept for 3 0 m i n

have been m o b i l e art (CONARD & UERPMANN

utes u n d e r v a c u u m of < 2 0 0 m b a r (Vacutherm

1999).

chamber, Heraeus I n s t r u m e n t s ) .

T h e samples

important

were removed from the v a c u u m chamber, c o m

game. In a d d i t i o n , the layers contain bones o f

pletely i m m e r s e d in the resin mixture a n d then

m a n y other m a m m a l s , a m o n g which fox a n d

put back into the chamber w h e r e they were kept

hare are a b u n d a n t .

for 5 days under v a c u u m , followed by a 2 4 - h o u r

Horse a n d reindeer were t h e most

heating period at 60° C . After i m p r e g n a t i o n ,

PAUL GOLDBERG, SOLVEIG SCHIEGL, KAREN MELIGNE, C H R I S DAYTON & NICHOLAS J . CONARD

Fig. 4: Photograph of Profile 2 showing plaster-jacketed sediment samples. Compare with Figure 3.

several 1 to 2 cm-thick slices were cut from each

bined M i c r o a n a l y z e r ) . Optical e x a m i n a t i o n of

block by m e a n s of a water-cooled rock saw. Sev

the thin sections consisted of observation w i t h

eral representative areas were chosen from

the

the microfiche reader at magnifications of ca. 10

slices for petrographic thin section preparation.

to 20x, a n d w i t h the petrographic microscope at

Two series of thin section were produced, large

magnifications that ranged from 2 0 x to 4 0 0 x .

sections of sizes of 7 c m x 10 cm for transmitted

Such a strategy allows the section to be v i e w e d

light microscopy and smaller ones (3.5 c m x 2 . 5

at different scales, ranging from field to h a n d

cm) w i t h h i g h l y polished surfaces for scanning

sample d o w n to ultra-fine detail w i t h the S E M

electron microscopy.

(COURTY et al.

In a d d i t i o n to the sample blocks, a second se

T h e large thin sections were also scanned on a

ries of loose sediment were collected from cor

flat-bed

1989).

scanner (ARPIN et a l . 2 0 0 2 ) in order to

responding localities for infrared spectroscopy.

facilitate documentation

The latter were dried in a heating oven for sev

T h i s procedure

eral days at 60° C.

spots analyzed by the electron microprobe a n a

for the

enables efficient

microprobe. location

lyzer, a n d in turn correlate electron microscope Analytical M e t h o d s

data with those obtained t h r o u g h

Petrographic thin sections were observed w i t h

light microscopy.

polarizing

Polished t h i n sections of the

microfiche reader, transmitted polarizing light

undisturbed sediments were carbon-coated a n d

microscope, and electron microprobe analyzer

analyzed by Jeol Superprobe,

(Jeol Superprobe J X A - 8 9 0 0 R W D / E D

energy dispersive (ED)- and w a v e length ( W D )

Com

equipped

with

Micromorphology and Site Formation at Hohle Fels Cave, Swabian Jura, Germany dispersive-analytical techniques (see ScmrsGL et

subdivisions w i t h i n C to A, the m a i n units. T h e

al. in press, for details).

relevant subdivisions w i t h i n Gravettian U n i t C

Finally, some of the loose s a m p l e s of the b u r n t

are layers 3 c , 3b a n d their various subdivisions

material from Layer 3cf (Figure 3 ) were analyzed

(Tables 1 a n d 2; Figure 4 ) . U n i t B is c u l t u r a l l y

by Fourier Transform

Spectroscopy

sterile. T h e subdivisions w i t h i n U n i t A are Lay

(FTIR; Nicolet Avatar 3 6 0 FT-IR E.S.E, c o m

ers l k a n d 0 c a n d date to the M a g d a l e n i a n a n d

puter-controlled by O m n i c Version 5.1). F T I R

Holocene, respectively (Table 1; Figure 3 ) .

Infrared

spectra w i t h i n the w a v e n u m b e r - r a n g e between 4 0 0 a n d 4 0 0 0 cm"' were o b t a i n e d by the potas

Coarse Fraction

s i u m bromide (KBr)-pellet technique. Tens of

T h e coarse elements, defined as grains of sand-

micrograms of sample were finely ground using

size a n d larger (60 p m ) , consist of a n t h r o p o

an agate m o r t a r a n d pestle, a n d ca. 0.1 mg of

genic, geogenic, a n d biogenic components.

the sample powder was m i x e d w i t h about 8 0

anthropogenic elements are b u r n t bone, s o m e of

The

m g KBr (Uvasol by Merck, I R - g r a d e ) . A 7 m m -

the u n b u r n t bone (if modified by h u m a n s ) , pos

pellet was p r o d u c e d by m e a n s of a hand press

sibly coprolites, a n d charcoal.

w i t h o u t evacuation. T h e e m p t y sample chamber

ponents include limestone clasts a n d calcareous

Geogenic c o m

was used as reference background. T h i r t y - t w o

„Ornaments" w h i c h crystallized on the roof a n d

scans w i t h a spectral resolution of 4 cm"' spectra

walls a n d were then detached. Two c o m p o n e n t s

were carried out. If necessary, the baseline w a s

of the coarse fraction could be attributed to both

corrected for measurements of the peak absorb-

h u m a n a n d other biological agents: coprolites(/

ances. Infrared-sensitive constituents were iden

phosphatic grains?) a n d u n b u r n t bone. A few

tified using a reference library containing m o r e

other m i n o r constituents were observed in some

than 100 reference spectra relevant to archaeo

of the thin sections: quartz grains, iron particles,

logical samples.

and the coprolites m e n t i o n e d above. Bone, either burnt or u n b u r n t , is nearly u b i q uitous throughout the sediments, except in the 4 Results

culturally sterile Unit B (Table 2 ) . W h i l e w e found u n b u r n t bone in all the Gravettian a n d

Micromorphology T h e sediments from Hohle Fels Cave are more complex than they first appear on the macro scopic level in the field. T h e micromorphological e x a m i n a t i o n of 17 thin sections from units C through A reveals fine variations of the texture, fabric a n d organization of the m a i n constitu ents.

Overall, the sediments are characterized

by heterogeneity, which is itself expressed in different w a y s throughout the stratigraphic s u c cession. T h e basic components, calcareous clay, lithic fragments, bone, charcoal and some fine organic material, are consistent through most of the sequence, although their organization a n d proportion c h a n g e locally w i t h i n the deposits.

M a g d a l e n i a n layers, b u r n t bone was

present

in significant quantities o n l y in layers 3b, 3bt, and 3cf of the Gravettian period. T h e size of the bone fragments ranges from unidentifiable splinters (as small as 2 0 urn) to cm-long pieces. Several tooth fragments are also present

and

occur in the matrix or are incorporated w i t h i n aggregates (Figure 5 ) . A l t h o u g h they are m o s t l y rounded - likely by cryoturbation - some bone fragments in aggregates remain very sharp a n d angular, suggesting reworking a n d transport of m u c h of the bone (the significance of this bone layer is discussed below, a n d in detail in SCHIEGL et al. 2 0 0 3 ) . Charcoal is overall less c o m m o n

than

burnt

For the most part, the descriptions and discus

bone, being almost absent from the Gravettian

sion below refer to the geological/archaeological

sediments (Unit C ) and totally absent from the

PAUL GOLDBERG, SOLVEIG SCHIEGL, KAREN MELIGNE, C H R I S DAYTON & NICHOLAS J . CONARD

Tab. 2: Summary of Micromorphological Attributes of Sediments from Hohle Fels Cave

Bone

Charcoal

Textural Features

Fine Fractipn

Coarse Fraction Lithic

Non -solid patterns

Solid patterns

Samples by depth

HF-7A_top HF-7A middle HF-7A bottom

HF-7B top

HF-7B middle

Ch Ch"

HF-7B bottom

Magdalenian

phLS

uLS

phLS

°-

HF-12A top HF-12A middle HF-12A bottom uLS

HF-12Bbottom

HF-4Atop

HF-4A middle

uLS bB

uLS

uLs-

HF-4A bottom

üj~_r~_

HF-4B top

uLS

HF-4B middle

uB"" uB

uLS

HF-4B bottom

uLS

hlF-1 top

uLS

HF-1 middle

uLS

HF-1 bottom

phLS

Coa

uLS

HF-13 top

uLS

HF-13 middle

uLS

HF-13 bottom

uLS

HF-6 top

uLS

phLS

HF-6 middle"

uLS

phLS phLS phLS

HF-6 bottom

HF-8 (op

ulS uLS

HF-8 middle

uLS

HF-8 bottom

uLS _phLS

HF-5 junger top

uLS

HF-5 junger bottom

Cap DeCa clay

phLS

uLS

HF-5 Alter top

uLS

HF-5 Alter bottom

C Gravettian

uLS

uLSphLS

HF-12B top

B Sterile

uLS uLS 'uLS"

uLS"

HF-11Jop_

uLS

HF-11 middle

uLS

"uls"phis

HF-11 bottom

HF3A~5P—

HF-9A middle

uLS _ _ _ _ _

HF-9A bottom

WWW

uLS ÜLS~"phIs

HF-9B middle

uLS

HF-9B bottom

uLS

HF-3Atop

uLS

HF-3A middle

uLS

HF-3Ä bottom

uBbB

ÜLS^

HF-3B top

uLS

HF-3B middle

Ü B -

uLS

HF-3B bottom

uLS

HF-3C log

Cap Cap

DOCA

uLS

HF-3C middle HF-3C bottom

a n t h r o p o g e n i c a l l y sterile sediments of

phLS

uLS uLS "

Layer

charcoal fragments, w h i c h range in size from a

B (Table 2 ) . W i t h i n the Gravettian sequence,

few microns to a few m i l l i m e t e r s . T h e s e frag

only o n e layer contains significant a m o u n t s of

ments are either incorporated into the fine frac

charcoal:

tion or c o n t a i n e d w i t h i n r o u n d e d

Layer 3 a d at the top of the Gravet

tian sequence. O n the other hand, most of the

(Figure 5 ) .

M a g d a l e n i a n sediments ( U n i t A ) were rich in

portion

these

charcoal

aggregates

fragments

are

1 1

Micromorphology and Site Formation at Hohle Fels* Cave, Swabian Jura, Germany

Fig. 5: Microphotograph of coarse, sand-sized clasts incorporated within rounded aggregates in sample HF-4B (Layer 3b). In particular, note the presence of charcoal fragments and rodent tooth in the center of the photograph. Plane-polarized light (PPL); width of view, ca. 3.2 mm.

Fig: 6: Microphotograph of sample HF-3C (Layer 3c) showing partially phosphatized limestone grain revealed by slightly lighter color on left and upper part of the grain (P with arrows; this is yellow-brown in color photograph). PPL; width of view, ca. 3.2 mm.

from

cross-polarized light ( X P L ) . In ultraviolet light,

Holocene

beech (Fagus)

deciduous

trees, particularly

a n d have been reworked

into

the M a g d a l e n i a n deposits. Fragments of b i r c h {Betula)

a n d w i l l o w {Salix)

appear to be

the phosphatized

porrions

fluoresce

strongly,

while the n o n phosphatized limestone „core" of

the grains does not. Phosphatic replacement of

Pleistocene o r i g i n (These w e r e identified b y S.

calcite is also manifested by tooth-like, etched

Riehl. T h e masses of beech clearly stem from

t e r m i n a t i o n s of calcite (Figures 7a, 7 b ) .

Holocene features).

phatization of calcareous g r a i n s does not appear

T h e A u r i g n a c i a n layers ( U n i t D; analyzed by

to follow a specific stratigraphic pattern, a n d it

Freddy D a m b l o n in Brussels) have birch, p i n e

m a y be that phosphatization occurs in localized

a n d even beech. T h e presence of the latter s u g

areas t h r o u g h o u t the entire sequence. A m b e r -

gests a w a r m interstadial d u r i n g this t i m e ; its

colored

occurrence in the M a g d a l e n i a n - a cold p e r i o d

but likely biogenic, origin occur in all samples

- is clearly intrusive.

(Table 2; Figures 8a, 8 b ) .

The

lithoclastic c o m p o n e n t

consists

phosphatic

grains of

Phos

indeterminate,

almost

exclusively of limestone fragments, and s o m e

Fine F r a c t i o n

calcareous ,ornaments' (cf. crystalline features

T h e fine fraction consists of a y e l l o w - b r o w n to

below).

brown calcareous and locally phosphatic clay.

Diverse types of limestone are present

throughout

the

sediments,

including o o l i t i c

Rare silt size inclusions of q u a r t z grains, a m b e r -

a n d d o l o m i t i c limestone. T h e y vary from s a n d

colored phosphatic grains, a n d organic material

to pebble size, a n d from s u b a n g u l a r to r o u n d e d .

- as well as silt-size fragments of the b o n e a n d

An interesting feature of s o m e limestone frag

charcoal described above - are e m b e d d e d w i t h i n

ments is their partial phosphatization,

the clay.

which

is manifested in plane polarized light (PPL) by

Although

a yellow-brown reaction r i m along the e d g e of

t h r o u g h o u t the sequence, the matrix in Layer

the grain (Figure 6 ) ; these r i m s are isotropic in

3c clearly differs from that of a n y other layers

this

calcareous

clay

present

PAUL GOLDBERG, SOLVEIG SCHIEGL, KAREN MELIGNE, C H R I S DAYTON & NICHOLAS J . CONARD

Fig. 7a: Microphotograph of phosphatized and etched calcite grain from sample HF-3C (Layer 3c). Etching of the calcite and replacement by phosphate creates an tooth-like pattern on the edge of the grain. PPL; width of view, ca. 650 pm.

Fig. 8a: Microphotograph of slightly darker, amber-colored phosphatic grains in sample HF-8 (Layer 3b). Note their isotropic nature and the siltsize inclusions of quartz in XPL. They appear to represent phosphatic clays that have been reworked by cryoturbation or movement of material from within the main hall of the cave. PPL; width of view, ca. 650 pm.

Fig. 8b: XPL.

(Table 2 ) . Layer 3c is characterized by localized

ized a n d seems to be an exception. T h e d o m a i n s

d o m a i n s of decalcified clay that appear w i t h i n

of decalcified clay are therefore characteristic of

the g e n e r a l l y calcareous m a t r i x (Figure 9a, 9 b ) .

Layer 3 C only.

T h e frequency of the decalcified d o m a i n s d e 足

As discussed below, the dip of the deposits from

creases u p w a r d within L a y e r 3c, from s a m p l e

the interior of the cave to the exterior clearly i n 足

H F - 3 C to the m i d d l e of s a m p l e HF-3A. A n

dicates that the clay is derived from the interior

isolated zone of decalcified matrix is also ob足

of the cave.

served in s a m p l e HF-8 ( L a y e r 3 b ) but it is local足

u l t i m a t e l y derived from soil materials that w e r e

Moreover, the clay appears to b e

Micromorphology and Site Formation at Hohle Fels Cave, Swabian Jura, Germany

Fig. 9a: Sample HF-3C (Layer 3c). Microphoto足 graph of a domain of decalcified clay within the generally calcareous matrix. While the matrix appears undifferentiated in plane-polarized light, crosspolarized examination reveals distinct domains of isotropic, decalcified clay. This decalcification of the matrix occurs only within Layer 3c of the Gravettian complex. PPL; width of view, ca. 3.2 mm.

Fig. 10: Microphotograph of the loose, nonaggregated calcareous clay matrix within a moderately developed platy void structure in sample HF-3C (Layer 3c). The platy structure is created by ice lensing. PPL; width of view, ca. 1.6 mm.

Fig. 9b: XPL

Fig. 11: Microphotograph of loose rounded aggregates in sample HF-3A (Layer 3b/3c) resulting from cryoturbation. The individual rounded aggregares are clearly separated and non compacted. PPL; width of view, ca. 3.2 mm.

washed into the cave through openings in the

Fabric

roof, one of w h i c h can be seen at the back of the

As discussed above, the fine fraction is generally

interior of the cave today.

heterogeneous calcareous clay w h o s e fabrics c a n

However, we w e r e

u n a b l e to obtain a n d analyze a n y modern soil

be described as c o m b i n a t i o n s of a small n u m b e r

material from the slopes above the cave since

of solid p a t t e r n i n g (matrix) a n d non-solid pat足

these slopes w e r e denuded in historical (likely

terning (voids). W e divide the solid patterning

Medieval) times.

into four m o d e s of organization a n d the n o n solid p a t t e r n i n g into three m o d e s .

PAUL GOLDBERG, SOLVEIG SCHIEGL, KAREN MELIGNE, C H R I S DAYTON & NICHOLAS J . CONARD

Solid patterning:

1 ) T h i s is simply a loose non-ag

gregated m i x of clay and inclusions (Figure 1 0 ) . 2 ) T h e second type is characterized by clearly defined individual rounded aggregates or ,loose rounded

aggregates' (Figure 1 1 ) . These

indi

vidual aggregates in some cases have a core c o m posed of a coarse component, such as a fragment of bone, charcoal, or lithic material (see Figure 5). 3 ) In this case, the aggregates are compressed into m o r e massive c o m p o u n d subangular ,macroaggregates' (Figure 1 2 ) . In such instances, the overall microstructure of the matrix is fissured or subangular blocky, and pedality of the material is evident. 4 ) Finally, the matrix also occurs as a massive, non-aggregated form, where the clay is

Fig: 13: Microphotograph of massive, non-aggregated and generally homogeneous clayey matrix associated with fissures and cracks from sample HF-8 (Layer 3b). PPL; width of view, ca. 3.2 mm.

relatively homogeneous compared to the type 3 , above (Figure 1 3 ) . unpatterned,

displaying

irregular

interstitial

(packing) voids between singular and c o m p o u n d aggregates (Figure 1 1 ) . 3 ) T h i s last form is char acterized by fissures a n d cracks (Figure 1 2 ) . In all thin sections e x a m i n e d , platy voids are generally encountered either w i t h the loose nonaggregated matrix (Figure 1 0 ) or w i t h the loose rounded aggregates (Figure 1 4 ; Table 2 ) . Van Vliet-Lanoe (VAN VLIET-LANOE 1 9 8 5 ) reports that platy structure due to ice lensing is best ex pressed in homogenous s a n d y substrates. In the case of Hohle Fels the heterogeneity of the sedi Fig. 12: Sample HF-7B (Layer l k ) . Microphotograph of massive subangular macroaggregates associated with fissures and crack structure. The matrix, bounded by the fissures, are constituted of cryoturbated, rounded aggregates compacted together with some looser matrix material. P P L ; width of view, ca. 3.2 mm.

ments a n d the presence of large coarse elements - p r i m a r i l y and ultimately products of roof fall - makes the ice lensing structure less evident. However, the platy organization is still visible in localized domains. T h e interstitial void structure is mostly an at

In a d d i t i o n , three types of non-solid patterning,

tribute of the loose rounded aggregates (Figure

i.e., organization patterns of the voids are very

1 1 ) , a n d both patterns are characteristic of the

informative.

1 ) T h e first type is characterized by

effect of cryoturbation (VAN VLIET-LANOE 1 9 8 2 ,

elongated voids, which give the matrix - whether

1 9 8 7 , 1 9 9 1 , 1 9 9 8 ) . Fissures and cracks, on the

aggregated or not - an overall platy appearance

other hand, are associated w i t h both the massive

(Figure 1 0 ) . As discussed below, such void struc

subangular

ture results from ice lensing and is a typical m a n

with the massive non-aggregated matrix (Figure

ifestation of frost activity preserved in sediments

13).

macroaggregates

(Figure

1 2 ) and

and soils (VAN VLIET-LANOE 1 9 8 2 , 1 9 8 5 , 1 9 8 7 ,

In this context of extreme heterogeneity, the dif

1 9 9 8 ) . 2 ) Here, the void structure is relatively

ferent types of fabric tend to coexist w i t h i n the

Micromorphology and Site Formation at Hohle Fels Cave, Swabian Jura, Germany

Textural features T h r e e varieties of textural or

post-depositional

features can be observed in thin section. Each type entails finely bedded matrix material - clay, organic matter, and fine lithic, b o n e and char足 coal fragments

- redistributed

around

coarse

elements, such as aggregates or limestone clasts. T h e principal types of textural features include 1) coatings around the entire m a r g i n s of coarse grains, 2) cappings on upper surfaces (Figure 16) a n d pendents on lower surfaces. Most coatings a n d cappings are poorly sorted, although they are finely bedded, except for overall coarser cappings Fig. 14: Sample HF-11 (Layer 3b). Microphotograph of loose rounded aggregates within an overall platy void structure. The platy structure, caused by ice lensing, is superimposed on a matrix that has already been subjected to cryoturbation. PPL; width of view, ca. 3.2 mm.

in sample H F - 5 , which are constituted of sorted, inversely graded matrix material (Figure 1 7 ) . T h i c k cappings are characteristic throughout the Gravettian 3b unit (Table 2 ) . T h e pendents are rare, as they were observed only in samples H F 12 and H F - 1 3 , both located on the tight side of the profile, a w a y from the central axis where most of the samples were taken.

Fig. 15: Sample HF-4B (Layer l k ) . Microphotograph of a contact zone between two different types of fabric, illustrating the extremely high variability of fabric types within a single sample. Isolated rounded aggregates occur in the lower portion, whereas the upper part of the photo shows more compacted, massive matrix material with fissured microstructure. PPL; width of view; ca. 3.2 mm.

Fig. 16: Microphotograph of a thick, finely bedded silty capping in the central part of the photograph resting on a clast of oolitic limestone that makes up the lower half of the photograph; sample HF-3A (Layer 3b). PPL; width of view, ca. 3.2 mm.

same thin section c o m m o n l y being found a d 足

Crystalline features

jacent to one another (Figure 1 5 ) . W i t h i n each

Samples H F - 4 ,

sample, however, it is possible to identify general

from the M a g d a l e n i a n layers (Layers Oc and l k ) ,

fabric trends, as discussed below.

as well as sample HF-1 from the sterile Layers

HF-7,

and H F - 1 2 ,

collected

PAUL GOLDBERG, SOLVEIG SCHIEGL, KAREN MELIGNE, C H R I S DAYTON & NICHOLAS J . CONARD

Fig. 17: Microphotograph of a poorly sorted coarse capping, consisting of quartz silt, rounded silt size phosphatic grains and aggregates and opaque minerals in black. Sample HF-5 Alter (Layer 3b). PPL; width of view, ca. 650 pm.

Fig. 18: Microphotograph of a microlayered calca reous ,ornament'. Note the finely bedded precipitate with irregular form . The precipitate was originally arranged around a limestone clast (see remains fragment of oolitic limestone, bottom left). It either represents a broken pendent formed on the underside of rock resting on the floor of the cave, or more likely was probably detached from the walls or ceiling of the cave. Sample HF-7B. PPL; width of view, ca. 3.2 mm.

(Is a n d 3 a s ) , contain t w o types of c r y s t a l l i n e

most examples of this crystalline feature have

features, calcareous o r n a m e n t s and calcific ac

irregular shapes, a few are well r o u n d e d .

The

c u m u l a t i o n s that were not observed in other

m i n e r a l o g y is consistent w i t h their m o i s t , pasty

layers.

feel in the field, similar to that of m o o n m i l k consist of finely

(GILLIESON 1997: 117, 1 2 2 , 1 2 6 ) . T h e s e crys

bedded calcareous precipitates in the form of

talline features occur in the upper part of the

isolated fragments or of coatings a r o u n d l i m e

stratigraphic section, m o s t l y in Layers Is, 3as

stone g r a i n s (Figure 1 8 ) . T h e y appear in finely

a n d l k (Figure 4; Tables 1 a n d 2 ) .

T h e calcareous , o r n a m e n t s '

deposited, u n d u l a t i n g beds, and produce c a u l i flower-like

formations. W h e n e x a m i n e d u n d e r

ultraviolet light, these calcareous precipitates

5 Discussion

are h i g h l y fluorescent, in contrast to the oolitic limestone fragments w i t h w h i c h they are often

In the field, minor lithostratigraphic differences

associated. These o r n a m e n t s appear to be frag

are evident in the exposed profile, m o s t l y d i s t i n

ments of material that precipitated a l o n g the

guishable by differing a m o u n t s of roof fall a n d

cave w a l l s , similar to stalactites, that later w e r e

slight color changes in the matrix. In general,

dislodged from their original e n v i r o n m e n t

the s e d i m e n t s appear to be similar (see Table

the w a l l s or ceiling of the cave.

1 a n d Figure 4 ) . However, e x a m i n a t i o n of the

T h e s e c o n d crystalline feature appears c r e a m y

thin sections provides a m u c h greater level of

white in PPL, and w h i t e to gray u n d e r X P L

resolution, revealing n u a n c e d differences

and is a calcite precipitate (identified by F T I R

provide significant insight into the geological

and S E M ) (Figures 19a, 19b, 19c). A l t h o u g h

history of the cave deposits. T h e overall pattern

that

Micromorphology and Site Formation at Hohle Fels Cave, Swabian Jura, Germany and 4 ) .

Nevertheless, the textural,

17 composi

tional and fabric data demonstrate that climatic conditions - a n d their

fluctuations

- that existed

outside the cave can be inferred from trends in these sediments. T h e current floor of the cave is about 2 m h i g h e r than it w o u l d have been in Gravettian t i m e s due to subsequent deposi tion of geological a n d anthropogenic material. Therefore the cave entrance w o u l d have been approximately 5 meters high in total, exposing it more fully to conditions outside and m a k i n g the nature of the deposits m o r e sensitive to c l i m a t i c variations. T h e main hall of the cave has been h e a v i l y modified

in historic times

by „mining" for bear bones, phosphatic sedi ments, and by use as a m i l i t a r y storage depot d u r i n g the S e c o n d World War; in the interior hall, therefore, h i g h quality Paleolithic data are not

available. However,

of climatic information

given the

amount

preserved along

the

entrance passage, it seems likely that climatic variations also w o u l d have affected the m a i n hall of the cave. Unfortunately, in the case of H o h l e Fels this information is probably lost; the exact nature of frost activity inside the m a i n hall remains u n k n o w n . Based on available evidence, Fig. 19 a+b: Sample HF-7B (Layer lk/Oc) is from the upper part of the Hohle Fels profile, which is typically lighter in color. The microphotograph illustrates irregularly shaped, sub founded precipitates of calcite, which are creamy white in PPL and white and gray under XPL. The surrounding fabric includes subangular macroaggregates associated with massive structure, fissures, and cracks, a) PPL, b) XPL; width of view, ca. 3.2 mm.

h u m a n activities seem to have been focussed in the entrance passage which w a s sheltered from the elements, but where a d e q u a t e daylight w a s available for diverse activities i n c l u d i n g stone k n a p p i n g and b o n e and ivory w o r k i n g . V i e w e d overall, o n e of the most striking features of the data is the clear unconformity w i t h i n the Gravettian o c c u p a t i o n between geological L a y ers 3c and 3 b (Table 2 ) . T h i s unconformity is

of the results is presented in Table 2. These pat

visible in t e r m s of decalcification and

terns reflect changes in climatic conditions, a n

phatization of the matrix, fabric, and textural

phos

thropogenic activity, and other depositional a n d

features, a l t h o u g h it is not evident in the

post-depositional processes discussed below.

dates. Layer 3c, represented by samples H F - 3 C ,

Climatic c o n d i t i o n s

l 4

HF-

3 B , and the lower portion of sample H F - 3 A ,

T h e profile from w h i c h these s a m p l e s were col

is marked by distinct decalcification of

lected lies w i t h i n the entrance passageway to the

clay matrix, w h i c h occurs in localized d o m a i n s

the

m a i n chamber of the cave, and is approximately

w i t h i n the calcified matrix (Figure 9 ) . S u c h

2 0 m from the actual cave e n t r a n c e (Figures 3

alteration suggests an episode in w h i c h the sedi-

PAUL GOLDBERG, SOLVEIG SCHIEGL, KAREN MELIGNE, C H R I S DAYTON & NICHOLAS J . CONARD

Mineralogie Tübingen

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FE UBS 4ch 1 M l Ka (I. .t-i I Pcok F.S.CHHO I34.B880

Fig. 19c: S E M B S E image of HF-7 with accompanying line scans shown in photo. Most of the scan is through the large, circular grain of calcite (cf. fig. 19a, b), but also includes grains of quartz (high Si peak) and bone (peak of P and C a ) . Iron is likely tied to the clay matrix.

Micromorphology and Site Formation at Hohle Fels Cave, Swabian Jura, Germany

m e n t s were exposed to w e a t h e r i n g under acidic

Moreover, it is difficult to ascertain t h e u l t i m a t e

conditions, p r e s u m a b l y associated w i t h the d e

source of the fine, clayey fraction of t h e sedi

cay of organic m a t e r i a l s (e.g., vegetal material,

m e n t s w h i c h m u s t have come from well inside

g u a n o ) . In contrast, the overlying sediments o f

the cave system. It is likely either relict karstic,

Layer 3b, represented b y samples H F - 1 1 , H F - 5 ,

phreatically-derived material a n d / o r soil materi

H F - 8 a n d H F - 6 , overall have a m u c h „fresher"

al that has w a s h e d through o p e n i n g s a n d joints

appearance microscopically. W h i l e these upper

in t h e cave. A t t e m p t s to locate t h e o r i g i n of the

sediments also c o n t a i n a significant phosphatic

fine fraction failed, i n part h a m p e r e d b y the fact

fine c o m p o n e n t , t h e phosphate is primarily in

that soil material w a s completely stripped from

the form of sand-size a m b e r grains that a t e i n

the slopes above t h e cave in M e d i e v a l times.

corporated into fabric structures (Figure 12).

U n t i l it was sealed i n t h e l 9 6 0 s , a small c h i m

Fabric differences also serve to distinguish Lay

ney near the back of the cave, w h i c h w a s just big

ers 3 c a n d 3 b . T h e samples from Layer 3c a r e

e n o u g h for people to climb t h r o u g h , connected

m a r k e d by loose, n o n - a g g r e g a t e d to loose aggre

the m a i n hall w i t h the hilltop above the cave.

g a t e d arrangements of matrix, often displaying

If this c h i m n e y existed d u r i n g t h e Pleistocene,

p l a t y voids (Figure 1 0 ) . These voids are charac

it helps to explain the source of t h e silt a n d

teristic of ice l e n s i n g i n northern regions (VAN

clay that contributed to the s e d i m e n t cone i n

VLIET-LANOE 1 9 8 2 ) , a n d have been used as

the m a i n hall a n d l e d to the oozing o u t w a r d

indicators of seasonal frost in cold paleoclimatic

m o v e m e n t of clay a n d silt that characterized t h e

reconstructions

overall s e d i m e n t a r y context of H o h l e Fels.

2001;

(e.g.,

CREMASCHI &

COURTY

VALLVERDU

VAN VLIET-LANOE1990;

Layer 3 b is also m a r k e d b y c a p p i n g s of fine

P i s s A R T e t a l . 1988a,. 1988b; VAN VLIET-LANOE

material on larger clasts, bones a n d aggregates.

1 9 9 1 ) . In the overlying Layer 3 b , however, t h e

S u c h capping c a n be explained i n terms of clay

m a t r i x is arranged i n loose r o u n d e d aggregates

migration

clearly separated b y interstitial/packing voids,

VLIET-LANOE

during

that

the spring

thawing (VAN

1 9 8 5 ) , a n d confirms

that t h e

by a

sediments near the entrance o f t h e cave were

p l a t y microstructure (Figures 11 a n d 14). Such

repeatedly exposed to freeze-thaw cycles d u r i n g

r o u n d e d aggregates a n d the general absence o f

this time.

in certain cases is superimposed

ice lensing features point to cryoturbation (VAN VLIET-LANOE 1 9 8 2 , 1987, 1 9 9 1 , 1998). More

over, the platy v o i d structure observed in t h e sediments of L a y e r 3 b is superimposed on t h e already-present cryoturbated matrix, a n d sug gests a later phase of ice lensing. It is difficult to d e t e r m i n e a specific t i m e frame for the duration of these processes as these processes can occur on the scale of seasons to decades. C r y o t u r b a t i o n a n d the clear d i p of the deposits from the m a i n c h a m b e r toward the entrance (Figures 3 a n d 4 ) is responsible for transport o f material from inside t h e cave ourwatd.

Unfor

tunately, d u e to modifications of the cave d u r ing the past century, a n d absence of excavation t o w a r d the interior, it is difficult to d o c u m e n t the physical connection between the two areas.

Finally,

the

unconformity

between

Layers

3c a n d 3 b is not visible i n t h e n u m e r o u s

l 4

dates from the deposits. T h e c l e a t b o u n d a r y between Layers 3 c a n d 3 b , a n d this hiatus sug gests that a n u n k n o w n portion o f 3 c sediments was removed d u r i n g this t i m e , l i k e l y after t h e decalcification of the layer b u t before active sedimentation of the overlying L a y e r 3 b w h i c h t o o k place in a regime of less e x t r e m e phosphate mobilization. A n additional trend in the results is the c o m b i n e d occurrence

of two calcareous crystal

l i n e features i n the sterile u n i t B a n d i n the M a g d a l e n i a n complex, unit A . In general, the M a g d a l e n i a n sediments are characterized b y a m o r e massive fabric of s u b a n g u l a r m a c r o a g gregates' a n d b y cracks a n d

fissures

(Figure

PAUL GOLDBERG, SOLVEIG SCHIEGL, KAREN MELIGNE, C H R I S DAYTON & NICHOLAS J . CONARD

12). W h i l e the c a p p i n g observed in L a y e r 3b disappears, coarse elements are often

thinly

coated a n d pendents occur in a few samples. The

crystalline features,

however,

are

most

noticeable. T h e y consist of fragments of cal citic cauliflower-like ornaments a n d

rounded

masses of calcite. But overall the p r o p o r t i o n of these two crystalline features is p a r t i c u l a r l y high in the sterile layer (Figure 2 0 a , 2 0 b ) , their concentration tends to increase u p w a r d s w i t h i n the M a g d a l e n i a n complex, w i t h o n l y rare traces in s a m p l e H F - 4 B (Layer l k ) a n d h i g h concen trations in sample H F - 7 B . 7 A (Layers 0 c a n d l k ) (Figure 4; Table 2 ) . T h e s e two features are entirely absent from the older, Gravettian lay ers, a n d the question of their u n i q u e presence in the u p p e r part of the sequence of the cave is i n t r i g u i n g a n d problematic. O n e interpretation Fig. 20a: Microphotograph of the calcareous and calcitic matrix of the sterile layers, sample HF-1 (Layer Is). The sample consists of bright, rounded masses of calcite and calcareous ornaments within a calcareous matrix. Nore the cauliflower-type aggregate in the lower part of the photo, and the platy piece of bedded flowstone in the center right. PPL,

is that they are related to a change of the overall c l i m a t i c regime of the area. As such, d r i p p i n g d u e to wetter a n d w a r m e r (i.e., less freezing) c l i m a t e could be responsible for the formation of both crystalline structures. T h e M a g d a l e n i a n predates the w a r m e r Bölling a n d A l l e r ö d peri ods w h i c h are then followed by the Younger Dryas cold period. However, the paragenesis of both of these secondary features is still u n d e r study. In sum, it is necessary to note that there is a substantial temporal gap at the L G M a n d the early dates for the Gravettian, c o u p l e d w i t h a relatively long period of

non-human-occupa

tion of the cave until ca. 13ka b.p.

A n t h r o p o g e n i c activity In the field, two m a i n phases of Paleolithic oc c u p a t i o n of the cave were identified b e t w e e n units A a n d C. Earlier occupation is attested in unit D , but there has been only l i m i t e d exca vation w i t h micromorphological d a t a for this older occupation. In thin section, h u m a n presence is manifested m a i n l y by the occurrence of bone fragments a n d charcoal. An interesting pattern e m e r g e d from the e x a m i n a t i o n a n d comparison of s a m p l e s Fig. 20b: XPL; width of view, ca. 3.2 mm.

from the M a g d a l e n i a n a n d from the Gravettian

Micromorphology and Site Formation at Hohle Fels Cave, Swabian Jura, Germany and

the

Gravettian

phases of occupation. C h a r c o a l is extremely rare

nian

in the Gravettian layers (Layer C ) , except from

suggests different pyrotechnological strategies.

occupation

layers

Layer 3ad, a dark layer situated at the very top of

T h e presence of b u r n t bone correlated w i t h the

the Gravettian sequence (Table 2 ) . M o s t of the

absence of charcoal in Layer 3b a n d partially in

Gravettian filling, therefore, is v i r t u a l l y devoid

Layer 3c, p r o b a b l y indicates the use of bone as

of charcoal. [S. Riehl has identified remains of

fuel d u r i n g the Gravettian. Bone fuel use has

w i l l o w {Salix)

in Gravettian layers. Based on

already been d e m o n s t r a t e d from the i n d e p e n d

charcoal, pollen a n d p h y t o l i t h s the Gravettian

ent study of a t h i n layer w i t h i n the Gravettian

is characterized by grasses and shrubs a n d seems

U n i t (SCHIEGI. et al. 2 0 0 3 ) . Layer 3 c f is a 3 to 10

to be a cool and d r y period. W i l l o w s are the

c m thick very d a r k layer of mostly burnt bone.

o n l y tree species thus far identified, a n d these

T h e m i c r o m o r p h o l o g i c a l investigation of Layer

are probably arctic shrub willow.] B u r n t bone,

3cf concluded that there was no evidence of in

on the other h a n d , is a b u n d a n t through Layer

situ

3 b and occasionally in Layer 3c of the Gravet

h a d been most likely deposited by d u m p i n g .

tian (Figure 2 1 ) . anthropogenic

T h e absence of charcoal in

sediments

containing

such

b u r n i n g a n d that the layer of burnt b o n e

Nevertheless,

the

extreme rarity of charcoal

w i t h i n the b u r n t b o n e Layer 3cf w a s confirmed.

evidence of b u r n i n g is certainly u n u s u a l . T h e

Our

reverse situation observed in the M a g d a l e n i a n

Gravettian c o m p l e x as a whole seems to confirm

m i c r o m o r p h o l o g i c a l e x a m i n a t i o n of the

layers, where charcoal is a b u n d a n t a n d burnt

the choice of b o n e fuel over charcoal during the

b o n e rare if not absent, m i g h t be considered

Gravettian o c c u p a t i o n of the cave. Schiegi et al.

more the expected case. (As m e n t i o n e d above,

(SCHIEGL et al. 2 0 0 3 ) review the w e a l t h of evi

some of the M a g d a l e n i a n charcoal

represents

dence for bone b u r n i n g during the M i d d l e Pal

especially the pres

aeolithic and U p p e r Palaeolithic of the Swabian

Holocene contamination, ence of a b u n d a n t beech.)

J u r a . O n the contrary, during the M a g d a l e n i a n

Such clear opposition

between the nature of

occupation, there are fewer signs of use of b o n e

anthropogenic remains present in the M a g d a l c -

fuel, but the presence of charcoal suggests use of regular w o o d as fuel. Finally, Layer 3 b t w i t h i n the Gravettian sedi m e n t s (Figure 4 ) w a s noteworthy in the sense that it c o n t a i n e d a very high d e n s i t y of b u r n t bone. T h e micromorphological s t u d y d e m o n strated the a n t h r o p o g e n i c / b i o g e n i c

nature

Layer 3bt w i t h i n the Layer 3b s e d i m e n t s , w h i c h are impoverished in charcoal. At least two of these dark pockets of burnt b o n e a n d charcoal w e r e seen in the profile (only one of w h i c h w a s s a m p l e d for analysis; Figure 4 ) . T h e burnt b o n e fragments range from slightly b u r n t to carbon Fig. 2 1 : Sample HF-9B (Layer 3bt).Microphotograph showing the concentration of burnt and unburnt bones mixed within a calcareous matrix which commonly coats the bones. This is most likely accumulated as dumped burned material (see SOLVEIG et al. 2003 for details). PPL; width of view, ca. 3.2 mm.

ized and microscopic fragments are mixed w i t h larger u n b u r n e d bone pieces (Figure 2 1 ) . T h e few

limestone clasts mixed w i t h the densely

packed burnt b o n e are u n b u r n t a n d exhibit a c a p p i n g s i m i l a r to that observed in the Layer 3 b sediments, suggesting that the formation of Layer 3bt took place during the Gravettian.

PAUL GOLDBERG, SOLVEIG SCHIEGL, KAREN MELIGNE, C H R I S DAYTON & NICHOLAS J . CONARD

Phosphate

from the food they b r o u g h t in or from their ex

Phosphatization of the matrix or fine fraction is

crements.

relatively h i g h both in the Gravettian s e d i m e n t s

intense use of the cave b y bears d u r i n g Gravet

(layers 3 b a n d 3c) a n d the M a g d a l e n i a n sedi

tian times. Bones of cave bear are b y far the most

ments (layers l k and Oc). T h e intervening sedi

numerous, and the age profiles are d o m i n a t e d by

ments (layer 3a where present, is a m i x e d layer

y o u n g a n d old a n i m a l s that usually die during

that separates l k from the Gravettian 3b layer),

hibernation (MONZEL et al. 2 0 0 0 ) . A

however,

phosphatized.

of m m to c m size pieces of carnivore coprolites

ultraviolet light, the clay-rich m a t r i x

was found in the thin sections. A l t h o u g h these

Under

are

markedly

of Layer 3 c is homogeneously

fluorescent,

evi

There is v e r y good evidence for the

number

are too small to identify as to specific animal,

dence of its highly phosphatized and decalcified

bears are a likely c a n d i d a t e .

nature. A l t h o u g h Layer 3c includes r o u g h l y the

this point the details of the g e o c h e m i c a l and

same c o m p o n e n t s - clay, silt, limestone, bone,

microenvironmental conditions responsible for

and charcoal - as the layers above it, in Layer

decalcification and phosphatization of the ma

3c these elements are finer and more „worked

trix, movement of phosphatic solutions, and the

into" the matrix, either by physical or c h e m i

formation of phosphate

cal processes. As displayed in sample H F - 3 A ,

limestone clasts are not clear a n d are currently

Layer 3b contains a m u c h coarser assortment of

under study.

In a n y case, at

reaction r i m s around

these c o m p o n e n t s . T h i s contact is visible at the macroscopic scale as well. In the field, 3 b w a s

Conclusion

described as m u c h siltier and sandier - relatively

T h i s preliminary s t u d y of the M a g d a l e n i a n

devoid of clay - than the „argillaceous silt" of

and Gravettian s e d i m e n t s at H o h l e Fels dem

Layer 3 c .

onstrates the potential of m i c r o m o r p h o l o g i c a l

T h e k e y contact between Layers 3c a n d 3b is

study of archaeological deposits in cold regions,

also e v i d e n t in the occurrence of large grains

particularly this part of G e r m a n y w h i c h both

of p h o s p h a t i c

underwent

material in 3b in contrast

the relatively homogeneous

alteration of

to the

marked c l i m a t i c c h a n g e b u t also

contains a rich record of prehistoric occupa

matrix found in Layer 3c. Ultraviolet e x a m i n a

tions. Although it is l i k e l y that no o n e meth

tion of s a m p l e H F - 1 1 , taken from the lower

odological approach c o u l d hope to c o m p l e t e l y

part of Layer 3b, revealed dense

phosphatic

elucidate the complex a r r a n g e m e n t of anthro

grains. T h e s e grains c o u l d be the r e m n a n t s of

pogenic, biogenic, a n d geogenic e l e m e n t s de

a p h o s p h a t e crust derived from guano or other

posited

products

analysis provides information

of animal activity. T h e presence of

this

cave,

micromorphological complementary

intensive a n i m a l occupation would account for

to that gathered by traditional field a n d labora

the increased phosphatization of Layer 3 c . T h e

tory m e t h o d s (COURTY et al. 1 9 8 9 ) . T h e Layer

intensive h u m a n occupation and c r y o t u r b a t i o n

3c sediments display p l a t y structures indicative

of 3b c o u l d have broken up this ctust, incorpo

of m o r e continuous cold conditions. W h i l e the

rating r o u n d e d fragments of dense

phosphate

overlying Layer 3b s e d i m e n t s also c o n t a i n some

w i t h i n the overlying 3 b sediments, as found in

platy or lens-like structures, they are d o m i n a t e d

sample H F - 1 1 .

by r o u n d e d cryoturbation aggregates.

T h e source of the phosphate is not totally clear.

grains indicate a greater frequency of freeze/

However, the a b u n d a n c e of bear remains from

thaw cycles, a conclusion supported

in the interior of the cave - which must have

presence of cappings of fine m a t e r i a l on large

served as their hibernation home - w o u l d point

clasts a n d aggregates. F r o m the a n t h r o p o g e n i c

to bear as a possible source of phosphate, either

perspective, both Layers 3 c a n d 3 b are compat-

These by

the

Micromorphology and Site Formation at Hohle Fels Cave, Swabian Jura, Germany ible w i t h the use of bone as the p t i m a r y fuel, w h i l e higher in the sequence, charcoal r e m a i n s

Führer 1; B l a u b e u r e n : S c h r ö d e r . BURKF.RT, W

& FLOSS, FI. (in press): L i t h i c

i n d i c a t e the use of w o o d fuel instead (SCHIEGL

e x p l o i t a t i o n areas in the U p p e r Paleolithic

et al. 2 0 0 3 ) .

of W e s t a n d S o u t h w e s t G e r m a n y - a c o m

M u c h of this p r e l i m i n a r y w o r k will be refined as

parative study. VIII. - F l i n t S y m p o s i u m ;

m o r e exposures - both vertical a n d lateral - be

Bochum.

c o m e available at H o h l e Fels. In a d d i t i o n , w o r k

CAMPEN, I. ( 1 9 8 7 ) . Die S e d i m e n t e der H ö h l e n

at the c o n t e m p o r a r y site of Geissenklösterle

und Abris der M i t t l e r e n S c h w ä b i s c h e n A l b

a b o u t 2 k m a w a y will serve as a comparison to

und ihre klimatische A u s d e u t u n g . - D o c t o

e v a l u a t e a n d extend the observations a n d inter

ral dissertation; University of T ü b i n g e n .

pretations m a d e here. T h i s study adds further

CONARD, N . J . 6kBOLUS, M . ( 2 0 0 3 ) : R a d i o c a r b o n

e v i d e n c e to the discussion of h u m a n responses

dating the Appearance of M o d e r n

to c l i m a t i c c h a n g e in the U p p e r Paleolithic.

and the T i m i n g of C u l t u r a l Innovations in

Humans

W h e n results from the M i d d l e Palaeolithic a n d

Europe: N e w Results a n d n e w C h a l l e n g e s . -

earliest U p p e r Palaeolithic units from

Journal of H u m a n Evolution, 44: 3 3 1 - 3 7 1 ;

Fels

and

Geissenklösterle

Hohle

b e c o m e available,

w e w i l l have s o m e very clear notions a b o u t the environmental

b a c k g r o u n d at this

important

transition in h u m a n history.

Amsterdam. CONARD, N . J . & FLOSS, H. ( 1 9 9 9 ) : Ein b e m a l tet Stein v o m H o h l e Fels bei S c h e l k l i n g e n u n d die Frage nach paläolithischer H ö h l e n kunst

in M i t t e l e u r o p a . - Archäologisches

Korrespondenzblatt, 29: 3 0 7 - 3 1 6 ; M a i n z . CONARD, N . J . & FLOSS, H. ( 2 0 0 0 ) : Eine Elfen

6 Acknowledgments

beinplastik v o m H o h l e Fels bei S c h e l k l i n g e n We

w o u l d like to thank

Philipp

Drechsler,

Kurt L a n g g u t h , Laura Niven, A n d r e w del,

Kan-

T i m o t h y Prindiville, a n d Kirsten Schell

of the Institut für Ur- u n d Frühgeschichte u n d Archäologie

des Mittelalters der

Universität

u n d ihre B e d e u t u n g für die E n t w i c k l u n g des J u n p a l ä o l i t h i k u m s in S ü d d e u t s c h l a n d . - Archäologisches Korrespondenzblatt,

30:

473-480; Mainz. CONARD, N . J . & FLOSS, FI. ( 2 0 0 1 ) : N e u e Eiszeit-

T ü b i n g e n for their assistance in collecting the

Kunstwerke von der S c h w ä b i s c h e n A l b - In

u n w i e l d y samples used in this study. Ilean Isaza

KÖLBL, S. &

assisted w i t h collection of some of the m i c r o

Eiszeit-Kunstwerke von der S c h w ä b i s c h e n

m o r p h o l o g i c a l data.

Alb.

CONARD, N . J . [Eds.]: N e u e

Urgeschichtliches M u s e u m

Blaubeu

ten, M u s e u m s h e f t 4: 2 1 - 3 4 ; Stadt B l a u b e u ren u n d Institut für Ur- u n d Frühgeschichte der Universität T ü b i n g e n ; T ü b i n g e n .

7 References

CONARD, N . J . , ARPIN,

L.,

MALLOL,

GOLDBERG,

LANGGUTH, K. & U E R P M A N N ,

P. ( 2 0 0 0 ) : Die A u s g r a b u n g e n 1 9 9 9 in d e n

( 2 0 0 2 ) : A n e w m e t h o d of a n a l y z i n g a n d

Gravettien-Schichten

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