The Continental Record of Stage 11: A Review
Denis-Didier Rousseau
Paleoenvironnements et Palynologie, Institut des Sciences de VEvolution (UMR CNRS 5554),
Universite Montpellier II, Montpellier, France
AND
Lamont-Doherty Earth Observatory of Columbia University, Palisades, New York
The review of terrestrial records of marine isotope stage 1 1 indicates that they
are mostly yielded by pollen and loess sequences. They occur in different locali­
ties around the world and show different time resolution and environmental con­
ditions. Other records are discussed which correspond to more particular condi­
tions, i.e., the Lake Baikal deposits, or the terrestrial malacofauna from tufa de­
posits in Western Europe. If almost all the records indicate moister conditions
than present, the temperature estimates vary from similar to the present, to
warmer from place to place. Another problem related to the interpretation of ter­
restrial deposits of stage 1 1 is the time resolution and the sampling interval of the
related deposits that makes correlation with other proxies even more difficult due
to the long duration of this interglacial. However, a scenario is proposed to link
the different reviewed record based on a general warm climate of MIS 1 1 .
1.
INTRODUCTION
The continental stratigraphy of Europe is complicated
and there are conflicting interpretations about which
European terrestrial interglacial correlates with marine
isotope stage (MIS) 11 [Sarnthein, Stremme, and Mangini, 1986]. Kukla [in Smiley et al, 1991] demonstrated
by comparing marine and continental records, that MIS
11 corresponds to the terrestrial interglacial named Holsteinian in northern Europe (Figs. 1, 2). Most workers
have now adopted the correlation of MIS 11 with Holsteinian and I accept that correlation in this summary.
Identification of the continental equivalent of MIS 11
(Holsteinian) is most certain in continuous sequences that
Earth's Climate and Orbital Eccentricity:
T h e M a r i n e I s o t o p e Stage 11 Q u e s t i o n
Geophysical M o n o g r a p h 137
contain a complete sequence of superimposed climate cycles (Fig. 2). However the time resolution in the continuous sequences is not always fine enough to resolve detailed climatic and environmental changes that are present
in records from ice cores or high-accumulation rate marine cores. The lack of high-resolution terrestrial records
must be taken into account when comparing terrestrial records to ice core and marine records. The purpose of this
study is to review the most significant terrestrial records
of MIS 11. For convenience the records are
grouped
by
depositional
setting.
At least three well developed pollen series which record
the terrestrial equivalent of MIS 11 are known from
Europe. These are Plateau de Devres (Lac du BouchetPraclaux) in the French Massif Central, Ioannina 249, and
Tenaghi Philippon in Greece (Fig. 1). The variations of
Copyright 2003 b y the American Geophysical U n i o n
10.1029/137GM15
213
3($
214 CONTINENTAL RECORD OF STAGE 11: A REVIEW
F i g u r e 1. L o c a t i o n o f t h e d i f f e r e n t r e c o r d s d i s c u s s e d i n t h e t e x t . F i l l e d c i r c l e s c o r r e s p o n d t o i n d i v i d u a l l o n g s e ­
quences, f i l l e d squarres correspond to the occurrence o f the E u r o p e a n m o l l u s k localities
isotope stage
(Lyrodiscus b i o m e )
of marine
11.
AP (arboreal pollen) curve, which mirrors the marine 8 0
curve, allow the recognition of climate cycles in which
interglacials are characterized high percentages of arboreal pollen (Fig. 3).
In the Plateau de Devres (Lac du Bouchet-Praclaux)
section, which is located at an elevation of about 1100m,
MIS 11 is correlated with the Holsteinian interglacial and
is locally named the Praclaux interglacial. Pollen zones
have been identified in the Plateau de Devres section
which describe a precise vegetation succession [Reille
and de Beaulieu, 1995] (Fig. 3). The beginning of the interglacial (Fig. 3, Zone 2) is marked by the simultaneous
expansion of Quercus and Corylus. The occurrence of
Acer, Ulmus, Fraxinus and Ilex indicate temperate climatic conditions. A short interval with the development
of Taxus (Zone 3) suggests moister and colder conditions.
In the overlying Zone 4, Abies expands strongly. However, the occurrence of Buxus, Vitis, and other thermophilous taxa clearly indicate continued temperate conditions, especially in summer. The overlying Zone 5 shows
the expansion of Fagus compared to Quercus whereas
Buxus and Abies reach their highest percentages. The end
of the interglacial is marked by the decline of Abies corresponding to cooler conditions although Pterocarya, a
thermophilous plant is still observed. The highest zone
(Zone 7) corresponds to a boreal forest. The interpretation
of this vegetation succession clearly indicates that the
Praclaux or Holsteinian interglacial included variable environmental and climatic conditions, not necessarily
18
warmer than younger interglacials, including the present
one, even if pollen grains of Buxus and Vitis indicate sustained temperature. On the contrary, Reille and de Beaulieu, [1995] suggest the pollen record of the Praclaux indicates moister conditions compared to the present.
A similar interpretation was derived from the analysis
of the pollen sequence at La Cote (1000m elevation), in
the French Alps [Field et al, 2000] where almost the
same vegetation succession was identified. Climatic estimates were derived from parallel investigation of pollen
and beetle remains. Although the optimum climatic conditions were interpreted as similar to modern conditions,
the coleopteran assemblages indicate that the peak interglacial was warmer and wetter than modern conditions.
The Ioannina 249 record was recovered from a plain at
an elevation of about 470m in Greece [Tzedakis, 1993;
1994; Tzedakis et al, 1997] (Fig. 4). MIS 11 is again well
developed and is correlated with two pollen zones, the
Dodoni I and II respectively. During this interval, the
pollen concentration is the highest observed in the record
and the pollen composition indicates the occurrence of a
dense forest environment. Both Dodoni I and II intervals
have high Abies percentages that differentiate them from
younger forest interglacials from this area. The lower Dodoni I is characterized by the dominance of Ulmus/Zelkova (the highest values for the entire sequence)
with also high percentages of Buxus. In contrast, Dodoni
II is characterized by the expansion of Quercus with Tilia
and Corylus. In addition the important taxa in the Dodoni
ROUSSEAU
OCEAN
LOESS
CLASSICAL SYSTEMS
N.AMERICA
AGE MIS
SPECMAP TER GLC
CK CHINA
C.USB
GL
INT
EUROPE
ALPS
GLAC
INT
F i g u r e 2 . C o n t i n e n t a l records o f M I S 1 1 . M a r i n e isotope stage 1 1 a c c o r d i n g to S P E C M A P
(Imbrie et al,
1984) and
c o m p a r i s o n w i t h the loess (European, general and Chinese), N o r t h A m e r i c a n , E u r o p e a n A l p i n e , and N o r t h E u r o p e a n
P l a i n Quaternary stratigraphies (after K u k l a i n
Smiley et al.,
1991 modified).
T E R : t e r m i n a t i o n s , G L C : g l a c i a l c y c l e s , C K : s t r a t i g r a p h i c p o s i t i o n o f terraces at R e d H i l l ( C z e k r e p u b l i c ) ,
C.USE:
current c o m m o n usage, G L : N o r t h A m e r i c a n glacials, I N T . : N o r t h A m e r i c a n interglacials, G L A C : N o r t h E u r o p e a n
g l a c i a t i o n s , I N T : N o r t h E u r o p e a n i n t e r g l a c i a l s . W I S : W i s c o n s i n i a n , S A N : S a n g a m o n i a n , 111. I l l i n o i a n , E . M . U . . I L L :
E a r l y , M i d d l e and U p p e r I l l i n o i a n , Y A R : Y a r m o u t h i a n , W : W u r m , R W : R i s s - W u r m , R: Riss, M R : M i n d e l - R i s s . F:
Faunal dispersal event.
F i g u r e 3 . L a c d u B o u c h e t p o l l e n s e q u e n c e , a, C o m p a r i s o n o f t h e A P ( A r b o r e a l p o l l e n g r a i n s ) - P i n u s p e r c e n t a g e s w i t h
the S P E C M A P 8
1 8
0 curve. I n d i c a t i o n o f the stratigraphy w i t h l o c a t i o n o f the Praclaux-Holsteinian interglacial ( f r o m
D e B e a u l i e u m o d i f i e d ) , b, S i m p l i f i e d p o l l e n d i a g r a m (selected trees) o f the H o l s t e i n i a n (after
1995 modified).
Reille andDe Beaulieu,
215
216 CONTINENTAL RECORD OF STAGE 11: A REVIEW
Depth
(m)
0
AP/NAP
(%)
Ap concentration
(x 1000 grains/cm )
3
Pollen
Zones
0 10 103040 0 10 2010 40 SO CO 0 0 10 200 0 0 10 0 10 2030 10203040 0 10 0
Marine Isotope
Stages
resenting humid and warm conditions passed to a pine
forest indicating increasing dryness. Then an evergreen
oak forest invaded the lower belts of the pine forest, followed by a mixed oak forest with carpinus, Tilia, Ostrya,
Fraxinus and Acer. The succession described in the
Lekanis interglacial is considered to represent a Mediterranean type of climax vegetation, which was not reached
in the following younger interglacials [Wijmstra and Smit,
1976].
Two additional long sequences from the Mediterranean
area come from Hula in northern Israel and Amazyabu 1
in southern Israel. In these sequences interglacials correspond to interpluvial periods with a strong influence of
the Sahara and therefore few rains originating from the
Mediterranean [Fuji and Horowitz, 1989; Horowitz,
1989]. The terrestrial equivalent of MIS 11 was identified
in pollen zone QVI. The pollen sequence indicates an evergreen oak forest with pine stands and a dry Mediterranean climate. Comparison between the northern and
southern Israel sites shows different environmental conditions implying a steep climatic gradient between north
and south (Fig 5). The vegetation in northern Israel indicates desert environment while southern Israel experienced steppe, i.e., moister conditions which is unlike today.
A long record (last 800 kyr) is preserved in the Biwa
sequence from Japan [Fuji and Horowitz, 1989]. The
01020 0 10
Figure 4. Pollen sequence at Ioannina (Greece), a) Variation in
the AP (Arboreal pollen grains)-NAP (Non Arboreal pollen
grains) percentage on the left, in AP concentration, pollen zones,
correlation with the marine isotope chronology, b) Simplified
pollen diagram of the Dodoni pollen zones (after Tzedakis, 1994
modified).
I interval are reduced in Dodoni II. The high pollen concentration of warm taxa such as Buxus, Ulmus, Zelkova,
and Alnus indicate high temperature conditions and the
presence of Fagus, indicates low precipitation and high
temperature conditions. The record of MIS 11 in Ioannina
249 is in complete agreement with the record from
Tenaghi, Philippon [Wijmstra and Smit, 1976; Wijmstra
and Yound, 1992] in Macedonia, north of Ioannima. The
Tenaghi record spans the past 975 ka and shows a strong
terrestrial biomass development during the Lekanis interglacial which is correlated with MIS 11 [Wijmstra and
Young, 1992]. Wijmstra and Young [1992] identified a series of pollen zones that represent the succession of
vegetation during the Lekanis interglacial. From the bottom up, an oak forest with Tilia, Ulmus and Fraxinus rep-
Figure 5. Comparison between the long terrestrial pollen records in Israel and Japan, pollen zones, and correlation with the
SPECMAP chronology (after Fuji and Horowitz, 1989 modified).
ROUSSEAU 217
a
4 High plain of Bogota
* Mag dale na river
*>• Xerophytic vegetation
Forest line
-
i
20b
600
8clo
H (1 1
2(A)
4(A)
6(A)
8(lo
1
lodo
Alnus
12(A)
1 .-III
lodo
14(A)
AP
(*)
12(lo
it
L
during the interval correlated with MIS 11 (Fig. 6), the
upper limit of the Andean forest was higher than 3000m
with a temperature higher than the present value of
14.8°C. Furthermore, a high percentage of Alnus is recorded which, in the Bogota area, is an indication of
swamps where Alnus mostly lives. Thus this high concentration could be interpreted as indicating more humidity but such a conclusion is speculative, as the lake level
at that time was low (Fig. 6).
The long record from Lake George in Australia also
contains an interval correlated with MIS 11 [Williams et
al, 1993]. However pollen is not preserved in the MS 11
interval so interpretations of temperature and vegetation
succession are not possible [Singh and Geissler, 1985],
However the MIS 11 interval of the core contains less
charcoal than younger interglacial intervals suggesting
fewer fires and thus possibly wetter conditions prevailed
during MIS 11 (Fig. 7).
Lake Baikal in Siberia provides another record of terrestrial conditions during MIS 11 [Williams et al 1997].
Data on biogenic silica flux measured in Lake Baikal
cores shows that the highest productivity and biogenic
14clo
Figure 6. Pollen sequence of Funza Bogota (Colombia), a)
Variation of the vegetation according to the present interglacial
and last glacial maximum scenarios, b) Variation of AP (Arboreal pollen grains) and Alnus percentages ( Alnus was excluded
from the pollen sum. This explains maximum values can reach
>100%) versus time. Indication of stage 11 interval (after
Hooghiemstra et al,. 1993 modified).
Biwa sequence shows that the vegetation succession during the different interglacials was similar to present conditions (Fig. 5). However pollen zone 9, which correlates
with MIS 11, indicates warmer conditions compared with
modern. Furthermore, the Biwa record indicates the presence of significant cooling within MIS 11 that is apparently coeval with the cold episode observed in the French
Lac du Bouchet-Praclaux sequence.
The Funza Bogota pollen sequence in Columbia, cored
from a plain located at 2550m elevation, contains a record
of the last 3.5 myrs [Hooghiemstra and Melice, 1994;
Hooghiemstra et al, 1993]. The AP curve indicates that
Figure 7. Comparison between SPECMAP isotope record and
the charcoal and pollen sequences from Lake George (Australia), (after Williams etal, 1993 modified).
which are now living only north of 6°S, and which were
absent from the area during younger interglacials. The
conclusion of this study is that the lagoonal and protected
embayments were warmer than the open marine environ218 CONTINENTAL RECORD OF STAGE 11: A REVIEW ments during this MIS 11 suggesting different conditions
than those prevailing at present or during other late
Pleistocene interglacials.
silica accumulation over the last 800,000 kyr occurred
The review of these coastal records leads to similar induring MIS 11. The long interglacial conditions of MIS
terpretations gained from the pollen records. Climate
11 in the Lake Baikal record abruptly ended at about 394
during MIS 11 was variable and there is no single pattern
- 390Ka due to a dramatic cooling in this region of South
of generally warmer conditions at all localities.
East Siberia. The abrupt cooling is thought to be caused
by a the response of continental Asia to insolation forcing
[Karabanov, et al, 2000]. The warm conditions are also
4. LOESS RECORDS
indicated by the occurrence of a dark coniferous forest
with Abies, Picea, Pinus sibirica which lately passed to a
Loess sequences provide another source of information
sparse steppe flora characteristics of glacial arid condion past climate change and terrestrial environmental contions.
ditions. Loess sequences mostly occur in the Northern
Hemisphere at the southern margin of the former iceIn summary the different pollen and lacustrine records
sheets or in the path of prevailing winds from regions of
reviewed here indicate variable temperature and moisture
persistent high pressure to low pressure cells. Loess seconditions around the world during MIS 11. The differquences that include several climatic cycles can provide
ences in time resolution of the individual records do not
permit detailed comparison between regions. Some recreliable records of past climatic changes. In China the
ords, especially those in Europe and Japan indicate that
Central Chinese loess plateau preserves a complete record
the terrestrial equivalent of MIS 11 includes several
of the past 2.4 Myrs in a series of stratigraphic units that
stages and at least one significant cooling.
can recognized across the entire plateau [ftukla, 1987].
Pal eomagnetic stratigraphy of the Chinese loess sequence
permits precise correlation of the loess sequence with ma3. COASTAL RECORDS
rine records.
1 (pollen
In the Ch inese loess sequence, MIS 11 is represented by
Zone 11) Afromontane forest trees expanded form higher
a soil complex named S4 within the Upper Lishi formato lower elevations twice (subzones l i d and b). Both extion [Kukla, 1987] (Fig. 2). Environmental information is
pansions were interpreted as corresponding to cool but
provided by measuring the iron oxide ratio which is an
more humid conditions during MIS 11 (Jahns et al.,
index of the weathering. The iron oxide ratio reflects the
1998).
percentage
of iron liberated from iron bearing silicate
Core GIK 16867-3 off Gabon, contains a record of the
minerals
through
chemical weathering [Guo et al, 1996,
last 700 ka. A maximum of lowland tropical forest (Al1998].
At
Changwu
(southern loess plateau) the iron oxchornea, Uapaca) expansion is recorded just at the end of
ide
index
in
soil
S4
reaches the highest values found in
MIS 12, before the transition to MIS 11. This transition is
the
loess
sequence
[Guo
et al, 1998] whereas at Xifeng
marked by the presence of Rhisophora indicating exten(100
km
northward),
the
iron
oxide ratio in S4 is lower. In
sion of the mangrove swamps along the coasts [Dupont et
fact
the
iron
oxide
ratios
in
S4
at Xifeng are lower than
al, 1998].
ratios
that
are
found
in
soils
considered
to be equivalent to
Pollen studies of the Rangitawa fossil beds, North West
the
last
interglacial.
The
interpretation
of
the MIS 11 iron
of Wellington in New Zealand, indicates that this unit was
oxide
ratio
data
is
that
compared
to
present
time, condideposited during MIS 11 under a warm and humid clitions
were
wetter
during
MIS
11
in
the
loess
plateau due
mate in shallow marine and estuarine environments. In
to
a
strengthened
summer
monsoon.
However
the inaddition, marine mollusk shell assemblages sampled in
creased
monsoon
was
not
strong
enough
to
carry
high
the same unit include taxa indicating warmer waters than
precipitation
to
Xifeng.
The
conclusion
is
supported
by
present [Bussell, 1986].
the
pollen
assemblages
in
Luochuan.
A
rich
pollen
asAs a final example, the multidisciplinary study of the
semblage with Anacardiaceae and Thalictrum lead Want
coastal deposits in northern Chile, at Mejillones Peninsula
et
al., [in Kukla, 1987] to conclude that the soil surface
(23°S) indicates a particularly warm climate in this area
during
S4 was wetter compared to the soils of the Lower
during MIS 11 [Ortlieb et al, 1996]. The interpretation is
Lishi
formation.
Thus the iron oxide ratio and pollen data
mainly based on the occurrence of marine mollusk species
ROUSSEAU
Changwu iron index
15
20
25
30
219
Marine
isotope
35
40
F i g u r e 8. V a r i a t i o n o f t h e w e a t h e r i n g i n d e x i n t e n s i t y i n t h e C h i n e s e l o e s s p l a t e a u , a ) L o c a t i o n o f t h e C h a n g w u s e ­
q u e n c e , b ) V a r i a t i o n i n t h e i r o n i n d e x r e p r e s e n t i n g t h e w e a t h e r i n g i n t e n s i t y ( a f t e r Guo
are compatible with the interpretation that a strengthening
of the summer monsoon regime during MIS 11 over central China carried enough precipitation, at least over the
southern belt of the Central loess plateau to induce a
strong weathering of the loess deposits (Fig 8).
5. A UNIQUE EUROPEAN FAUNAL EVENT
A sequence of loess and paleosols at St. Pierre-les Elbeuf in the Seine Valley, northwest France includes a record of MIS 11 [Lautridou and Verron, 1970]. The basal
unit of the Elbeuf IV soil complex, which is correlated
with MIS 11, is a tufa (Fig 9). The sediment overlying the
tufa contains a terrestrial malacofauna which has an unusual composition compared to the modern local fauna
[Rousseau, 1992; Rousseau, Puissegur, and Lecolle,
1992]. A similar malacofauna is found a few kilometers to
the east, still in the Seine Valley, associated with another
tufa deposit that has been dated by U/Th at - 4 0 0 ka. The
distinctive Elbeuf IV fossil assemblage has been found at
sites in Northern France, southeastern England (Hoxnian
age) and southwestern Germany. The distinctive assemblages are considered coeval and represent environmental
conditions that have no modern analogue in Europe. Forest species dominate the assemblages indicating temperate
conditions with high moisture. Some of the species still
occur in modern assemblages of the Seine Valley but others are now living in central Europe, some are southern
species (one is endemic to the Bayonne area) and one is
endemic of the northern part of the British Islands (Fig.
9). One extinct species in the MIS assemblage is related
et al,
1998 modified).
to a subgenus, Retinella (Lyrodiscus), which is currently
endemic to the Canary Islands [Rousseau and Puissegur,
1990]. Plant macrofossils associated with the Elbeuf IV
fossil assemblage include Mediterranean and tropical
trees including the Laurel of the Canary Islands. Using the
Biome concept, the Elbeuf IV assemblage was named the
Lyrodiscus biome. The composition of the Lyrodiscus biome indicates that the climate during the deposition of the
Elbeuf IV soil complex was warmer and moister than
modern conditions.
The different terrestrial records of MIS 11 summarized
in this report indicate variable climatic conditions from
generally similar too warmer than modern conditions. The
review also indicates that conditions were variable during
MIS 11. A marked north-south gradient apparently existed in Europe with higher temperature than today in
some places but generally more humid conditions in mid
latitudes and low precipitation in the Mediterranean basin.
The SE Asian monsoon was intensified and the high plain
of Bogota experienced hot and wet conditions. Warmer
than modern temperatures are indicated along the Chilean
and New Zealand coasts. A consistent pattern seen in the
terrestrial records is the indication of higher moisture (table 1). If more precipitation occurred over continental areas then increased evaporation should prevail in the
source areas (marine) and thus higher sea surface temperatures (SST). However few marine studies have provided evidence for higher SST during MIS 11 although
220 CONTINENTAL RECORD OF STAGE 11: A REVIEW
F i g u r e 9. E u r o p e a n m o l l u s k r e c o r d o f s t a g e 1 1 . a , S t P i e r r e - l e s - E l b e u f l o e s s s e q u e n c e b ) V e r n o n s e c t i o n s h o w i n g t h e
Lyrodiscus
Ruthenicafilograna;2 , Acicula polita; 3 , Laminifera pauli; 4 , Hygromiacinctella; 5 , Leiostyla anglica a n d
6 , Aegopis verticillus. T h e h a t c h e d z o n e i n d i c a t e s t h e d i s t r i b u t i o n o f t h i s p a r t i c u l a r b i o l o g i c a l a s s e m b l a g e . T h e p r e s e n t
d i s t r i b u t i o n o f Laminifera pauli i n e n d e m i c o f B a y o n n e a r e a ( S W o f F r a n c e ) a n d m a r k e d b y a n a r r o w
stratigraphic p o s i t i o n o f the deposits, c present d i s t r i b u t i o n o f m o l l u s k species b e l o n g i n g to the Stage 1 1
biome: 1,
a l : loess, a2: paleosol, 3: h u m i c soils, a4: f l u v i a t i l e sands, a5: f l u v i a t i l e gravels, a6: stone l e v e l , a7: "chocolat" level,
a8: b o t t o m o f the quarry, b l : chak (substratum), b2: rubefaction, b3: smooth facies tufa, b 4 : travertine, b 5 :
p l u m " tufa facies, b 6 : c o l l u v i u m . C I : m o d e m d i s t r i b u t i o n , c2: Stage 1 1
etal,
1992;
Rousseau,
Lyrodiscus b i o m e
distribution.(after
"sugar­
Rousseau
1992 modified).
T a b l e 1. S u m m a r y t a b l e o f t h e d i f f e r e n t c o n t i n e n t a l r e c o r d s o f M I S 1 1 d i s c u s s e d i n t h e p a p e r .
Area
Europe
Region
N . France-S England
Evidence for
observed climate
Age
Warmer and moister
Holsteinian
Source of evidence
Rousseau
etal,
1992
Rousseau, 1992
Plateau d e Deves
Warmer
temperature indi-
Hosteinian
cated b y the occurrence o f
Reille and de Beaulieu,
1995
Buxus a n d Vitis
Moister environment
L a Cote
Peak interglacial warmer
etal,
Hosteinian
Field
D o d o n i I a n d II
Tzedakis, 1993, 1994
2000
and moister than present
Ioannina
Dense forest environment
H i g h temperature
L o w precipitations
Tenaghi Philippon
Mediterranean
type
of
Lekanis
W i j m s t r a and Smit, 1976
climax vegetation
W i j m s t r a and Y o u n g , 1992
Stronger summer droughts
M o m m e r s t e e g et al.,
Higher winter rainfalls
1995
ROUSSEAU
221
T a b l e 1. C o n t i n u e d .
M i d d l e East
Israel
Reversed conditions (drier
Q V I pollen zone
i n the N o r t h a nd moister
Horowitz, 1989
F u j i and H o r o w i t z , 1989
i n the South) than today
Lake Baikal
East A s i a
Stage 11
Highest blooming: warmer
etal,
1997
W i l l i a m s et al,
2000
Williams
surface water temperature
K a r a b a n o v et a l . , 2 0 0 0
Warmer environment
Lake Biwa
than
Pollen zone 9
F u j i and H o r o w i t z , 1989
present
S W Pacific
etal,
C h i n e s e loess Plateau
Warmer and moister
Soil S4
Guo
Lake George
Moister ?
Stage 11
Williams
1998,1999
etal,
1993
Singh and Geissler, 1985
Rangitawa formation
W a r m e r surface
Warmer and more
Stage 11
Bussell, 1986
Pollen zone 7
Hooghiemstra, 1989
Stage 11
Ortlieb
humid
interval
Temperature
Funza Bogota
South A m e r i c a
higher
than
present
H u m i d i t y higher?
Mejilloves Peninsula
Tropical Africa
evidence
for
[Poli et al,
11
C o o l but moister climate
P o l l e n z o n e 11
J a h n s e f f l / . , 1998
Stage 11
D u p o n t e r a / . , 1998
3
grove
northward
advection
of
1999;
McManus et al,
between global climate during M I S
during
The
differences
11 and today.
How­
ever development of detailed and well-dated records i n
n u m b e r o f areas is r e q u i r e d b e f o r e a reliable
of
Atlantic
1999].
s u m m a r y presented here suggests some clear
a
reconstruc­
tion of climate and climate variability during M I S
11
can
be accomplished.
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16776
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