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RUSSIAN JOURNAL OF EARTH SCIENCES, English Translation, VOL 1, NO 1, DECEMBER 1998
Russian Edition: JULY 1998
Postglacial tectonics of the Baikal rift
K. G. Levi1, V. D. Mats2, Yu. S. Kusner3, P. G. Kirillov1, A. M. Alakshin4, S. V. Tolstov3, E. Yu. Osipov2, I. M. Efimova2, S. Bak5
1 Institute of the Earth’s Crust, Siberian Division, Russian Academy of Sciences,
2Institute of Limnology, Siberian Division, Russian Academy of Sciences,
3Institute of Geochemistry, Siberian Division, Russian Academy of Sciences,
4GGP “Irkutskgeofizika”,
5University of Potsdam, Germany
Introduction
Many phenomena related to sedimentary basins and adjoining mountainous areas of the Baikal rift zone have not been adequately interpreted, as yet. These are widespread occurrence of continental sands in rifting basins of the Baikal region, (their formation was traditionally associated with the maximum glaciation in the middle Pleistocene, but now it is considered as a strati-graphic element encompassing the whole Pleistocene and including deposits of various genetic types and various climatic phases [Bazarov et al., 1982; Logachev et al., 1974; Mats, 1987; Olyumn, 1961]); moraines that occur at depths of 300-400 m below the water level the Lake Baikal on its Barguzin slope, which may imply a lower lake level existing at that time [Galkin, 1975]; terraces on the Ushkan’i Islands, much more numerous as compared with four terraces on the lake bank [Lamakm, 1968] (the origin of the “superfluous” ones need be explained, but the number of shore terraces may also exceed ten, in which case they should be correlated with the terrace levels of the Bol’shoi Ushkanii Island [Eskm et al., 1959]); and the unexplained presence of exotic boulders on the Olkhon and Ushkan’i Islands [Bukharov and Fialkov, 1996], as well as in certain eastern coastal areas of North Baikal. Also surprising are abnormally high velocities of recent vertical movements (RVM) of the Earth’s surface in areas of a Pleistocene ice field [Logachev et al., 1974], tectonic fractures in glacier structures, and other phenomena. On the whole, these phenomena suggest that the North Baikal region may have experienced glacioisostatic movements similar to those presently observed in Fennoscandia and on the Canadian shield. We will discuss recent geological constraints on the Baikal glaciations and neotectonic deformations consistent with glacioisostatic movements and present
©1998 Russian Journal of Earth Sciences.
Paper No. TJE98004.
Online version of this paper was published on July 20 1998. URL: http://eos.wdcb.rssi.ru/tjes/TJE98004/TJE98004.htm
a numerical model of the lithosphere at the postglacial stage of its evolution in the Baikal region.
Pleistocene Glaciation
The problem of glaciation in the Baikal region has been debated beginning from the works by V. D. Cher-skii, P. N. Kropotkin, and others. Obruchev [1953] noted the presence of glacier structures in the Baikal region. Afterwards the presence of glaciers in the past was proven, and their dimensions and stages of their development have been established. More detailed data on these natural phenomena are reported in a number of works [Baikal Atlas, 1993; Bazarov, 1986; Bazarov et al., 1982; Kulchitskii, 1967; Lamakm, 1968; Logachev et al., 1974; Salop, 1964]. Geological and geomorpho-logical studies revealed the existence of four glaciations, the most intense and oldest of which is the Samarovo Glaciation [Kulchitskii, 1967].
The maximum glaciation (300-250 ka) covered a vast territory in the Baikal region [Logachev et al., 1974], but a more or less monolithic ice cap that covered the northern Baikal basin and adjacent ranges (Figures 1 and 2) is most pertinent to the purposes of our paper. The ice field was not continuous.
The underlying surface was comparatively smooth. Fragments of the end moraine belt indicate the glacier to cover an area of more than 100 000 km2. Ice tongues descended from mountains outward, toward the areas surrounding the Baikal rift zone, and inward the North Baikal depression.
Maximum glaciation moraines existed on the western and eastern flanks of the North Baikal basin (Figure 3), and their radiocarbon ages are presented in Table 1.
On the western North Baikal coast, a buried 90-m thick moraine was drilled through at depths of 17 to 106 m below the present level of Lake Baikal [Kulchitskii, 1967]. To the east, the Samarovo moraines, extending into the lake water area for more than 7 km, have been traced to depths of 350-400 m. They are supposed to have formed under subaerial conditions [Galkin, 1975], because morphologically expressed moraines of recent
Figure 1. Map showing the rates of recent vertical movements of the Earth’s surface and the reconstructed field of maximum glaciation in the Baikal region.
glaciation, developed under subaqueous conditions, are unknown. Then, the lake level considerably dropped some 300 ka.
Younger glacier structures include those of the late mid-Pleistocene (Taz stage) and early Late Pleistocene (early Ermakov stage, 80 ka and later) and have similar relationships with Baikal terraces. At greater distances from the shore zone, they form surfaces that preserve specific features of the glacier relief. In the near-shore zone, their surfaces experienced abrasion and show the plane relief of Baikal terraces. The latter are developed at levels of 150, 80, and 35-50 m. As is observed in the Tyya Promontory, in bank bluffs from the Kurla Head to Tyya River mouth, at both heads of the Frolikh
Cove, in the left-hand divide area of the Biramya River near its mouth, and at several other places, intricate facial relationships characterize deposits that compose the terraces: lacustrine, glacial-lacustrine, and glacial boulder loams are overlain by lacustrine deposits and covering loam with relict lake pebble. Overall, this group of glacial deposits is characterized by close association with lake deposits. The latter include widespread frost involutions and clastic material with clasts as large as gigantic blocks (bearing obvious traces of glacial abrasion) .
Thus, general synchronism has been established between glacial structures and Lake Baikal deposits (occasionally including endemic diatoms), and the moraine
Figure 2. Schematic map showing pre-Baikal sand deposits and reconstructed lake depressions (with the use of the scheme constructed by G. S. Goldyrev in 1982): 1 - outline of the contemporary Lake Baikal basin; 2 - paleobasin outline; 3 - sand deposits comparable with the Middle Pleistocene Krivoi Yar sands (a) within and (b) outside the paleobasin contour; 4 - delta deposits of the Selenga River.
relief in the shore contact zone of Lake Baikal has been reworked as a result of abrasion. The penetration of lake Baikal facies into glacial ones appears to reflect specific relationships between the lake water and glacier tongues during the deglaciation period. The age of these formations is determined from geological and geomorpho-logical evidence, findings of remnants of large mammal species specific to the middle Pleistocene in the section of a 80-m terrace [Bazarov, 1986], and radiocarbon datings (> 57 ka) of 40-m terrace deposits, Tyya Promontory (Table 1).
Younger moraines are widely developed on the shores of North Baikal (Figure 3). Their characteristic feature is a well-preserved ensemble of bottom, side, and end moraines and fluvioglacial boulder-pebble and lake
plains behind and ahead of the front of end moraines. They are evidently younger than the glacial structures associated with 30-50-m terraces; river and Baikal terraces as high as 20-25 m are leaned against or occasionally inset in the latter. The above glacial features may include two age groups: late Markov, as old as 50 ka (moraines of the Tampuda, Shegnanda, Kichera, and other rivers; a few dates are presented in Figure 3 and Table 1) and Sartan, younger than 25.88 ± 0.35 ka. The Sartan structures are mainly represented by cirque glaciers that only occasionally advanced into the Baikal shore zone.
As seen from the above data, the most important characteristic of glacial structures of the maximum glaciation is its discontinuous occurrence, weak (by far weaker
Figure 3. Schematic map showing glacier features of northern Baikal and related ages determined during the field works of 1996 and 1997.
Table 1. Radiocarbon datings of glacial and postglacial formations
Nos. Ages Locations and references
1 6790±120 Paleofan of the Molokon River, northern Baikal (BA 29/07 NA1) [this work]
2 7180±50 Rel-Slyudyanskoe constructional field, northern Baikal (turf overlying an ice lens;
BA 05/08 SL1) [this work]
3 10850±60 Frolikh Bay, northern Baikal (BA Fr-2) [this work]
4 25880±350 A rhinoceros bone from a submoraine surface, Rel River (SOAN-289) [Mats, 1987]
5 34350±60 Moraine in the Kichera River valley, northern Baikal (BA Ki-2) [this work]
6 39240±1780 Tompinskaya moraine, Omogachan Promontory, Baikal (SOAN-1626)
[Popova et al., 1989]
*BA - Beta Analitic Inc. Germany
*SOAN, Analytical laboratory, OIGGiM, Siberian Division of the Russian Academy of Sciences.
than at the postglacial stage) differentiation of the underlying surface, and occurrence of the Baikal basin moraines below the present level of the lake. The latter is difficult to explain without the assumption on a lower position of the lake water level at the Samarovo time. However, the drilling results from deep sea holes on the submarine Akademicheskii Ridge [Kuz’min et al., 1997] show that this drop in the lake level may have been insufficient in order that the ridge area including the BDP-96 drillhole site at sea depths of 300-350 m emerged above sea level. The level drop was accompanied by tectonic subsidence of the lake bottom and uplift of its shores [Dem’yanovtch et al., 1988; Logachev et al., 1974; Obruchev, 1953; Salop, 1964]. Post-maximum glacial features in upland cis-Baikal areas occur in deep (to 1000 m) valleys cutting the exaration surface of maximum glaciation, which implies a considerable tectonic uplift postdating the maximum. Study of the whole complex of glacial and lake deposits yields evidence of considerable post-glacial reworking of the relief.
Deformations of Late Pleistocene and Holocene Deposits
Morphological variability of active faults and their spatial relationship with sedimentary sequences and relief forms, varying in age and including those of the glacial and postglacial origin, suggest their classification into three age groups [Dem’yanovtch et al., 1988].
The first group includes deformations of relief elements related to faults; activation of these faults is dated at the beginning of the Late Pleistocene-Holocene stage. They are most clearly expressed as offsets in end moraine fronts marking a maximum advance of glaciers into the Baikal shore zone (Tyya Promontory) and in glacial deposits of the 80-m terrace [Dem ’yanovich et al., 1988]. Because of limited occurrence of mid-Quaternary forms in the contemporaneous relief, recognition of such faults encounters considerable difficulties. Faults active since the late Pleistocene have been discovered
in the delta area of the Verkhnyaya Angara River, near the Verkhnyaya Zaimka settlement, and within the Rel-Slyudyanskaya constructional plain. Moreover, echo-sounding survey showed that end-moraine amphitheaters occur at considerable depths all along the Bar-guzin shore and extend into the lake water area for more than 7 km, implying high activity of tectonic movements in the late Pleistocene [Sizikov and Levi, 1987]. Repeated reworking of existing benches by later movements explains the fact that relief forms associated with the faults of first group have been poorly preserved.
The second age group includes faults that deform terraces of the first Late Pleistocene glaciation; these terraces are widespread along the Baikal shore. Deformations of this group are observed in mouths of the Muzhinai and Molokon Rivers, in the mid-course of the Kichera River, in the Tompuda River mouth, along the southeastern boundaries of the Bolsherechensko-Davshinskaya and Sosnovsko-Tarkulikskayadepressions, in the Snezhnaya River mouth, and so on. The activation of fault motions in the Baikal shore zone was accompanied by reconfiguration of the shoreline and lake transgression that has left signatures in the second (6-8 m) Baikal terrace. Along shores of the Tyya-Goremykskoe plateau and Barguzinskii Range, the back suture of the terrace obliquely cuts the end-moraine amphitheaters and higher levels of fluvioglacial, alluvial, and lacustrine aggradation. At the foot of the Pri-morskii and Baikalskii Ranges, fault scarps of this age are overlain by piedmont alluvial fans. This age group may also include movements that offset deposits of the Karginsky-Sartan age (50-12 ka), including those dated by the radiocarbon method.
The third age group of discontinuous deformations includes “fresh” ruptures on the northwestern lake shore (Kurla Head), associated with the epoch of the late Zyryanka (Sartan, 24-12 ka) glaciation dated from archaeological evidence [Endmkhmskii, 1982]. Existence of these movements is debatable in the topography of eastern shore zones, but they did take place in the Selenga River mouth, where a fault-line scarp bounding
the contemporaneous river delta on the south began to form at that time. On the whole, the shoreline configuration changed insignificantly, and transgression features of the first (2-4 m) Baikal terrace formed in the Holocene are less pronounced than in terraces of higher levels. An exception is lowland aggradation banks in large river mouths, where active permafrost degradation was in progress at the Pleistocene-Holocene boundary time and large areas of Sartan (24-12 ka) terraces may have been completely reworked by thermal abrasion processes. Probably, some of the thermal abrasion and thermal erosion benches trace fault zones that are thermal water sources. Such a formation mechanism of benches that bound boggy basins may be responsible for the topography features observed at large piedmont promontories of the Baikal Range, in some delta areas of the Verkhnyaya Angara River between the Lake Baikal and Verkhnyaya Zaimka settlement, and on the isthmus of the Svyatoi Nos Peninsula.
The faults that were active in the Late Pleistocene-Holocene have significantly affected the lake shoreline configuration. The latter appears to be controlled by the relative orientation of fault zones and along-shore drift movement, particularly at places where loose Pleistocene deposits are involved in the shore formation process. Thus, Baikal and delta terraces in the Tyya and Slyudyanka mouths and in the Selenga delta are truncated by linear, NE trending benches of tectonic and abrasion origin. All this is evidence of rather intense tectonic processes at the Baikal deglaciation stage of the middle and late Pleistocene, and we cannot exclude the possibility that vertical tectonic movements were affected by the glaciation.
Estimation of the Barguzin Glacier Parameters
In the light of the aforesaid, the thickness of the Barguzin half-covering glacier, which existed in the northern part of the Lake Baikal, is of particular interest. The knowledge of contemporary glaciers provides means for estimating this thickness. As shown below, it is convenient to consider ice as a viscous solid body which flows under the action of gravity [Landau and Lifshits, 1965] but rather strictly preserves the relation between its area dimensions and thickness; under this approximation, contemporary glaciers are described by equations of the type
Hg = 96.95“17 (1)
where Sg is the glacier area (in km2) and Hg is the ice shield thickness (in km), with the correlation coefficient being r2 = 0.625 at the sample size n = 70. Substituting an approximate value of the glacier area (in our
case, determined from the end moraine belt of maximum glaciation) into equation (1), we obtain an approximate ice sheet thickness of about 700 m. This value is not much divergent from a geological-geomorphological estimate of about 400 m, obtained from the height of trough valleys [Logachev et al., 1974].
For comparison, we present the estimated sizes of present continental ice covers of Antarctic and Greenland [Dolgushtn and Osipova, 1989]. The general area Sg of the Antarctic ice sheet is 13 589 000 km2, and its average thickness Hg is = 2450 m, with a maximum of 4700 m. For the Greenland ice sheet, the respective values are 1 726 400 km2, 1790 m, and 3416 m. Note that if these ice caps were removed from the Earth’s surface, the internal sea at the place of Antarctic would have a depth of about 1500 m, and in the case of Greenland the depth would be about 800 m. Although the North Baikal glacier is not so large, it could ignificantly affect the underlying surface.
In our case there is enough evidence to suppose that, during the maximum glaciation period, the Lake Baikal level was lower by 300-400 m. This hypothesis is illustrated in Figure la. As seen from the figure, the Lake Baikal consisted of three connected or even isolated reservoirs at a time of 300-400 ka. Then, the water circulation in these reservoirs and therefore landscape environment essentially differed from those presently observed. A lower lake water level in the glaciation epoch is additionally supported by the fact that certain archaeological monuments (e.g. Ulan-Khada) have been destroyed as a result of their slow submersion below the lake level.
Large dimensions and total mass of the ice cover suggest the existence of glacioisostatic movements in the Baikal region. However, in order to verify the postglacial Baikal rift uplift, one should exclude the possible influence of gravity effects on the RVM rates of the Earth’s surface. Below, we briefly consider the spatial pattern of both gravity and RVM velocity anomalies, based on geodetic data.
RVM Velocity Anomalies as Constrained by Geodetic Data
The RVM in situ measurements performed in the early 1990s provided a basis for constructing an RVM scheme on the territory of the Baikal rift zone. A rather complicated pattern of RVM anomalies is observed in the area where the ice half-sheet lay. However, to a first approximation, two NE-trending bands of anomalies are recognizable; the anomalous RVM are positive in one of the bands and negative in the other. The first extends from the Svyatoi Nos Peninsula to the Verkhnyaya Angara basin, and the second extends from
the Olkhon Island to northern slopes of the Verkhnean-garskii Range and bounds the first band to the west. The first, positive-anomaly band is separated into several anomalies. Of those, three anomalies are most pronounced: the northwestern, most intense one is observed above the Verkhneangarskii basin and adjacent mountains of the Delyun-Uranskii and Severo-Muiskii Ranges (maximum rates are +27.4 mm/yr in the Verkhnyaya Angara head area and +16.3 mm/yr at the Yanchuya River source); central anomaly above the Kichera basin (+8.9 mm/yr in the Kichera River head area); and southwestern anomaly above the Barguzin Range, Svy-atoi Nos Peninsula, and southern Baikal Range (rates range from +0.2 to +8.8 mm/yr). Interestingly, the above maximums are confined to the most conspicuous traces of glaciation. The second band of negative anomalies is divided into at least four anomalies the largest of which trends northeast and is contiguous to the largest positive anomaly. This negative anomaly is observed above the eastern Verkhne-Angarskii Range, and its downward velocities reach 14.6 mm/yr in the Konkudera River head area. The rest of the anomalies, bending round the group of positive anomalies on the west, extends southwest through the Synnyr and Yng-dar Ranges, crosses the axis of the Predbaikalskii basin, and ends at the Olkhon Island. Here, mean velocities of downward movements amount to —2 mm/yr. Obviously, these anomalies cannot be attributed to glacioiso-static movements, but they imply the presence of a complex mechanism in which both gravity-density inhomogeneities of the lithosphere and tectonic differences between various morphostructural elements may be main disturbing factors.
Many of the gravity anomalies spatially correlate with the anomalies of RVM velocities, and this correlation is either positive or negative. Undoubtedly some of the anomalies coincide with areas of isostatic adjustment, so that postglacial vertical movements are likely to occur in the Baikal region, but their intensity is by far smaller as compared with Fennoscandia and other regions with a similar Pleistocene history of development.
Deep Structure of the Crust and Upper Mantle Under the Baikal Rift
In order to estimate physical properties of the material on which the ice shield lay and which was involved (probably is still involved) in glacioisostatic movements, one should roughly assess the depth at which the ice load removal was accommodated. The accommodation depths of the crust and upper mantle are likely to have been associated with lower strength characteristics and higher ductility. Seismic soundings of the crust and upper mantle in the Baikal region yield evidence of at least
three lower-strength layers that change seismic velocities [Artyushkov, 1993]. The shallowest inhomogeneity occurs at depths of 12 to 20 km and nearly coincides with the concentration area of seismic sources in the Baikal region; the next one is observed at depths of 35 to 50 km; and the deepest is the asthenosphere, whose roof occurs, according to various estimates, at depths ranging from 50 to 90 km. Another important fact is that earthquake sources in the Barguzinskii Range area are recorded down to depths of 55 km, whereas their usual depths in Baikal rift crust are as large as 35 km. Which of the inhomogeneities could have accommodated the ice load?
The answer to this question is not trivial, because the linear dimensions and mass of the Barguzin glacier are too small. The presence of abnormally deep (to 55 km) earthquake sources in the area where the ice thickness was highest and where abnormally high RVM rates are presently observed indicates that the subcrustal inhomogeneity was undoubtedly involved in the ice load adjustment process, because otherwise relatively ductile rocks at these depths would have inhibited the growth of seismogenic faults. However, from the standpoint of formal logic, the involvement of the intracrustal inhomogeneity in accommodation of the ice load also raises no doubts.
Thus, in our opinion, the available information is adequate for estimating the following important characteristics:
• minimum linear dimensions and mass of a glacier which can give rise to noticeable glacioisostatic movements;
• possible limiting dimensions of ice sheets of the Earth at given mean values of its physical parameters;
• possible amplitude of postglacial movements in the Baikal region;
• and viscous properties of those zones of the Baikal crust and mantle that are responsible for the glacioisostatic adjustment.
Model Estimates of Physical Parameters
In order to construct models of the postglacial uplift, one should estimate its characteristic linear dimensions L and height H. For this purpose, we represent the model postglacial uplift as a rectangular parallelepiped whose base area Sg=L2 and height H are such that L 3> H. According to empirical relation (1), this inequality is valid for all of the presently existing glaciers to a large degree of reliability.
To construct such a model, we consider the lithosphere as a very viscous fluid, and the process itself of the postglacial uplift, as a hydrodynamic attenuation of a strongly elongated disturbance of the length L on a plane boundary of an incompressible fluid of high viscosity ?y. Then, we obtain the equation
r) =
pgL 2?r
(2)
<7 = GUik + rj
dUjk
dt
(3)
dU,
____^ u_ ^ u
dt t L/v’
L/v for the “hydrodynamic” time
(4)
where we have r and v is the characteristic rate of uplift. Then, equation (3) for an isotropic stress assumes an essentially simpler form:
<r ={G+-)U,
T
(5)
In order that the viscosity and elasticity of the body in question might be values of the same order, the following condition must be satisfied:
T] = Gt (6)
Returning to the model adopted for the uplift area, the main condition L H gives
dL
~L
2 H ~L~
(7)
and hence the stress tensor can be written as
weight 17 = base area =
P9HL2 dL 2 H
= ^^ = ^ = gt = g—,
Then, the required dimensions of the uplift area can be estimated from the formula
where p is the mean crustal density within the uplift area, g is gravity, and r is the postglacial uplift time in the area considered. In our case we have p = 3.03 g/cm2, L = 320 km = 3.2 x 107 cm, and r = 30000 years = 9.5 x 1011 s. The substitution of these values into (2) gives T) = 1.3 x 102° poise, which is somewhat smaller than the estimates for Fennoscandia and Canadian shield [Artyushkov, 1993], but consistent with previous estimates for the Baikal region [Levi and Sherman, 1995].
However, formula (2) is not advantageous for estimating the dimensions of the postglacial uplift area L, since it relates two poorly defined quantities which are L and ?y. Therefore, we try to derive an equation relating L to easily estimated physical characteristics of the lithosphere; for this purpose, the latter will be considered as a high-viscosity solid [Landau and Lifshits, 1965]. Then, the stress tensor of such a body is defined by a general formula
L=^
pg
(9)
Equation (9) is self-consistent, because formula (2) can be readily obtained through eliminating G from (5) and (6). Adopting G k, 2.8 x 1011 dyne/cm2 and p k, 3.03 g/cm3 for rocks composing the lithosphere in the Baikal region, we obtain L Pd 220 220 km, which agrees with observations. The same equations give an estimate of the characteristic minimum size of a glacier capable of producing glacioisostatic movements. Its characteristic size cannot be smaller than 25 km. On the other hand, the thickness of a very large glacier cannot exceed, on average, 3.5 km, because otherwise it would crush its own base.
To estimate the possible postglacial uplift amplitude, one should know the ice density pg, density of the underlying substrate p, and thickness of the ice shield Hgy which we assume, for simplicity, to be 1000 m. This is a reasonable estimate, because equation (1) gives only an average value of Hg. Then, the equation
where G is the elastic modulus of the lithosphere, and Uik w dL/L are strain components. For our estimates, it is sufficient to consider the simplest case of a homogeneous isotropic lithosphere and to replace the hydrodynamic derivative in (3) by the estimate
H=—Hg
P
0.25 Ha
(10)
gives an uplift height of 200-300 m, which agrees reasonably well with the amplitude estimates of Late Quaternary tectonic movements from North Baikal morphome-tric data based on the river system incision depth and sedimentation rates [Levi et al., 1981]. The uplift rate may be estimated from the equation
V = H/t. (11)
Deglaciation Rates of the Sartan Ice Sheets and Some Problems of Human Paleogeoecology
Presently, the deglaciation history of the Baikal region cannot be determined due to poor preservation of end moraine ramparts of maximum glaciation, which prevents the delineation of glaciation geographical boundaries. Based on the available geological and geophysical evidence, the time variation of deglaciation over the past 40 thousand of years can be, to an extent, reconstructed. Below, we shortly discuss this problem.
Vershinnaya
Figure 4. End moraine series in the Kichera River valley, northernmost Lake Baikal (after [Osadchii, 1989]): 1 - reliable (a) and tentative (b) boundaries of the maximum glaciation; 2 -stadial moraines preserved in the contemporary relief; 3 - alluvial-lacustrine plains in “flooded” (a) and eroded (b) areas of stadial moraines; 4,5- glacial-lacustrine plains: dry (4) and swampy (5); 6 - lakes.
38,4 34,5 33,6 31,5 29,2 22,3 20,8 18,9 14,7 3,6 2,7
ka
Figure 5. Degradation intensity of the Kichera glacier, northern Baikal.
Presently, the Kichera River valley (northernmost Lake Baikal area) is the only place where some ten ramparts of end moraines are well preserved. These ramparts are geomorphologically well expressed, and relative age determinations date them at the early to latest Pleistocene [Bazarov, 1986]. In 1989, S. S. Osadchii mapped the entire system of the end moraine ramparts in the Kichera River valley and established their number to be 11-13; he assumed that the lowermost moraine fixes the spatial position of the maximum glaciation boundary, the glaciation age being about 300 ka as mentioned above. In 1994 and 1995, P. G. Kirillov and S. Bak determined an age of 34350 ± 60 years from the Cha-lauta moraine (Table 1), which dramatically diverges from the relative geochronology data reported by previous researchers. The scheme of Figure 4 (constructed after Osadchii [1989]) clearly shows considerable variation in the spacing between the moraine ramparts, implying that the glacier retreat rate correlated with climatic variations in the air temperature. In order to estimate the relative age of each moraine rampart, one should admit that the temperature rose uniformly. Given the validity of this assumption, each moraine may be dated from spacings between moraine ramparts. These simple considerations showed that the deglaciation rate varied with time (Figure 5), indirectly reflecting the climatic variations in the air temperature.
Now we briefly consider the intensity of soil formation in East Siberia during the past 50 k.y. The plot shown in Figure 6 was constructed using a collection of 14C datings (Appendix, Table 2). Furthermore, we
assumed that, in the case of global development of a phenomenon, the number of datings that fall into a given “time window” is maximum, whereas it is minimum if the process is depressed. The time window was taken to be wider than the standard deviation of the 14C determinations, and the windows overlapped, with a time step being 0.5. Simple calculations yielded a frequency curve, indirectly reflecting the climatic temperature variations in East Siberia; on the whole, this curve is consistent with the current geological notions (Figure 6).
Archaeological site datings in East Siberia (Appendix, Table 3) were processed in a similar way, and we obtained the site recurrence plot (which may show how often ancient peoples visited the Baikal region) illustrated in Figure 7.
Comparison between Figures 6 and 7 reveals an abnormally high recurrence of archaeological site datings during the Sartan glaciation in the Baikal region. The Holocene extremums may be explained by the general rise in temperature favorable for developing new lands by men. On the other hand, it is difficult to explain the frequent site occurrence during the Sartan time, when a rather cold climate dominated the Baikal region, and the ancient man was strongly dependent on environmental conditions. However, comparison of Figures 5 and 7 seems to resolve this contradiction. High déglaciation rates of the Sartan glaciers were characteristic of the time interval during which the Sartan archaeological sites were widespread. Thus, these facts, albeit indirect and somewhat insufficiently substantiated, yield
Years
Figure 6. Soil formation variation in East Siberia over the past 50000 years.
Intensity of variations, arbitr. units
om-^ctnooom-i^O'noo
90 1350 2610 3870 5130 6390 7650 8910 10170 11430 12690 13950 15210 16470 17730 18990 20250 21510 22770 24030 25290 26550 27810 29070 30330 31590 32850 34110 35370 36630 37890 39150 40410 41670 42930 44190 45450 46710 47970 49230 50490
ХЛГН 1VXIVH ЯНХ ЛО SOINOXOHX XVIOVXDXSOd :-TV ХЯ 1ЛЯ1
Figure 7. Recurrence of ancient people sites in East Siberia.
Number of sites
OtO-^CTNOOOtO-l^
2000 3200 4400 5600 6800 8000 9200 10400 11600 12700 13900 15100 16300 17500 18700 19900 21100 Kj 22300 | 23500 | 24700 25900 27100 28300 29500 30500 31700 32900 34100 35300 36500 37700 38900 40100 41300 42500 43700 44900
xxra ivxivH hhx xo soinoxoxx xviovxoxsod :-tv xa iahx
evidence of anomalous climatic conditions that existed in the Baikal region over the past 50 k.y. We hope that joint geological and geophysical studies that have been conducted since 1997 will provide final verification of these climatic features.
Future Development of the Postglacial Uplift Problem
The next stage in the elaboration of the problem of postglacial uplift in the Baikal rift zone consists in the intensity estimation of postglacial tectonic events as a function of the distance to the local center of the North Baikal glaciation. Deglaciation features in the region should correlate with stages of the Lake Baikal water level variation; thereby our knowledge of the mechanism responsible for the lake water discharge through the Angara River will be improved and many questions concerning the Pleistocene evolution of the region and regional climatic changes will be answered. Supposedly, the interpretation of terrace-like benches and terraces of the Ushkun’i Islands [Lamakm, 19521inkl3] can be beneficial to the solution of these and many other problems of the postglacial Baikal history.
Conclusion
Numerous traces of neotectonic movements and postglacial active tectonics have been reliably established in the Baikal rift zone. Substantial relief transformations postdating the maximum glaciation epoch are evidence of considerable tectonic uplift events with a highly probable postglacial component, which is additionally supported by relationships of the Bikal terraces of intermediate (35-50 and 80 m) and high (150 m) levels with glacial features. Subsynchronism of lake and glacial deposits and abrasion planation of the glacial relief at various levels can be most reasonably explained in terms of the glacier slide into the lake shore zone and, at the initial stage of deglaciation, abrasion truncation of the glacial relief which did not experience significant glacioisostatic uplift at that time. The glacioisostatic hypothesis is consistent with theoretical estimates obtained in this work.
Acknowledgements. We are grateful to Academician N. A. Logachev for a preliminary discussion and valuable comments. This work was supported by the International Science Foundation, grant No. RLG300; the International Association for the Promotion of Cooperation with Scientists from the Independent States of the Former Soviet Union, grant No. 93-014; the Russian Foundation for Basic Research, grant Nos. 95-05-14211, 96-05-64187, and 97-0596529; and the Siberian Division of the Russian Academy of Sciences, grant No. IGSORAN-97-22.
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Bazarov, D.-D. B., The Cenozoic of the Baikal Region and Western Zabaikal’e Area, Novosibirsk, Nauka, 1986 (in Russian).
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Endrikhinskii, A. S., The sequence of main geological events in southern Siberia in the late Pleistocene and Holocene, in Late Pleistocene and Holocene of Southern East Siberia, pp. 6-35, Novosibirsk, Nauka, 1982 (in Russian).
Eskin, A. S., Palshin, G. B., Grechishchev, E. K., and Galazii, G. I., Geology and some problems of neotectonics of the Ushkan’i Islands, in Proc. East Siberian Lnstitute, Siberian Division of Russian Academy of Sciences. Ser. geol., vol. 2, pp. 129-152, 1959 (in Russian).
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Kulchitskii, A. A., Maximum glaciation boundaries in the northern part of the West Baikal region, Voprosy Geologii Pribaikal’ya i Zabaikal’ya, 2(4), Chita, 298-301, 1967 (in Russian).
Kulchitskii, A. A., Deposits and paleogeography of the Baikal region during the maximum glaciation epoch, Geol. Ge-ofiz., 9, 60-67 (in Russian).
Kuz’min, M. I., Grachev, M. A., Williams, et al., Continuous paleoclimatic record over the past 4.5 m.y. (preliminary report), Geol. Geofiz., 38(5), 1021-1023, 1997 (in Russian) .
Lamakm, V. V., The Ushkan’i Islands and the Problem of the Lake Baikal Origin, Moscow, Gos. izd. geogr. lit., 1952 (in Russian).
Lamakm, V. V., Neotectonics of the Baikal Basin, Moscow, Nauka, 1968 (in Russian).
Landau L. D., Lifshits E. M. Theory of Elasticity, M., Nauka, 1965, 203 pp.
Levi, K. G., Kulchitskii, A. A., and Zubarenkova, L. P., Holocene tectonic movements in the central Goremyko-Tyiskii Highland, in Relief and Quaternary Deposits of the Stanovoe Upland, pp. 138-144, Moscow, Nauka, 1981 (in Russian).
Levi, K. G. and Sherman, S. I., Applied Geodynamics Analysis, Sciences Geologiques, 100, Tervuren, Belgique, 1995.
Logachev, N. A., Antoshchenko-Olenev, I. V., Bazarov, D. B., et al., Uplands in the Baikal Region, Moscow, Nauka,
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(Received May 15 1998.)
Appendix.
Table 2. The Holocene-Late Pleistocene age sequence of geological events in central Siberia
No. Stage Dating Location and references
1 Sub- 210±170 [Andreev, 1992)
2 Atlantic 430±30 Fernau stage moraines, Altai (SOAN-1427) (Endrikhmskii, 1982)
3 440±50 Fernau stage moraines, Altai (SOAN-1618) (Endrikhmskii, 1982)
4 430±50 Fernau stage moraines, Altai (SOAN-1616) (Endrikhmskii, 1982)
5 430±30 Fernau stage moraines, Altai (SOAN-1426) (Endrikhmskii, 1982)
6 525±100 Kargapolovo village, Ob River (SOAN-71) (Endrikhmskii, 1982)
7 540±25 Peat bog, Dzhasator River, Altai (SOAN-1756) (lvanovskn et al., 1982)
8 550±30 Yana River, below Ust’-Kuiga (GIN-655) (Kolpakov et al., 1980)
9 600±150 Megin-Kangalas district, Yakutia (Im-260) (Kostyukevich, 1980)
10 610±50 Fernau stage moraines, Altai (SOAN-1617) (Endrikhmskii, 1982)
11 715±140 Khara-Bugulunnyakh (Im-248) (Kostyukevich, 1980)
12 830±50 Peat bog, Dzhasator River, Altai (SOAN-1757) (lvanovskn et al., 1982)
13 870±60 Kirenga River (Vib-47) (Endrikhmskii, 1982)
14 910±120 (Andreev et al., 1992)
15 1090±135 Kargopolovo settlement, Ob River (SOAN-72) (Endrikhmskii, 1982)
16 1140±30 Peat bog, Dzhasator River, Altai (SOAN-1758) (lvanovskn et al., 1982)
17 1220±70 Tuva Upland (Beta-107352) (Arzhanmkov, this work)
18 1250±50 Pashino site (GIN-1742) (Laukhm et al., 1980)
19 1350±150 Ust’-Aldan district, Yakutia (Im-370) (Kostyukevich, 1980)
20 1400±100 Megin-Kangalas district, Yakutia (Im-354) (Kostyukevich, 1980)
21 1515±60 Kargopolovo settlement, Ob River (SOAN-73) (Endrikhmskii, 1982)
22 1610±70 (Andreev et al., 1992)
23 1670±65 Suzun River, Ob River tributary (SOAN-81) (Endrikhmskii, 1982)
24 2100±80 (Andreev et al., 1992)
25 2110±70 (Andreev et al., 1992)
26 2130±90 Suzun River, Ob River tributary (SOAN-28) (Endrikhmskii, 1982)
27 2170±60 (Andreev et al., 1992)
28 2180±100 (Andreev et al., 1992)
29 2230±100 Chadobets site, soil (KRIL-231) (Laukhm et al., 1980)
30 2270±80 Pashino site (GIN-1743) (Laukhm et al., 1980)
31 2300±10 Vitim River (Im-598) (Endrikhmskii, 1982)
32 2430±130 Selenga River delta, Dubrovino village (LG-142) (Endrikhmskii, 1982)
33 Subbo- 2520±80 (Andreev et al., 1992)
34 real 2650±100 (Andreev et al., 1992)
35 2680±60 Northern Middle Siberian Upland (GIN-498) (Bardeeva et al., 1980)
36 2780±90 Bytantai River (GIN-559) (Kolpakov et al., 1980)
37 2900±200 Ust’-Aldan district, Yakutia (Im-371) (Kostyukevich, 1980)
38 2970±40 Tumara, Kele, Tukulan, and Khandyga rivers (GIN-527) (Kolpakov et al., 1980)
39 2990±120 Chadobets site, (KRIL-232) (Laukhm et al., 1980)
40 3000±70 (Andreev et al., 1992)
41 3060±70 Bytantai River (GIN-551) (Kolpakov et al., 1980)
42 3160±100 (Andreev et al., 1992)
43 3200±40 Northern Middle Siberian Upland (GIN-497) (Bardeeva et al., 1980)
44 3200±100 Molodo River (GIN-1424) (Shofman, 1980)
45 3205±40 Peat bog, Dzhasator River, Altai (SOAN-1760g) (lvanovskn et al., 1982)
46 3215±20 Peat bog, Dzhasator River, Altai (SOAN-1759) (lvanovskn et al., 1982)
47 3250±70 (Andreev et al., 1992)
48 3280±130 Severnaya Zemlya Archipelago, (LU-1125) (Bolshiyanov et al., 1995)
49 3320±170 Markha River (GIN-901) (Shofman, 1980)
No. Stage Dating Location and references
50 3340±30 Bytantai River (GIN-550) (Kolpakov et al., 1980)
51 3370±200 Tumara River (GIN-532) (Kolpakov et al., 1980)
52 3390±30 Peat bog, Dzhasator River, Altai (SOAN-1760g) (Ivanovskn et al., 1982)
53 3400±90 Severnaya Zemlya Archipelago (LU-1123)(Bolshiyanov et al., 1995)
54 3600±130 Markha River (GIN-902) (Shofman, 1980)
55 3600±200 Markha River (GIN-900) (Shofman, 1980)
56 3600±80 Omoloi River, (GIN-847) (Kolpakov et al., 1980)
57 3610±100 (Andreev et al., 1992)
58 3790±50 Taimyr Peninsula (GIN-1154) (Nikolskaya et al., 1980)
59 3820±100 (Andreev et al., 1992)
60 3880±120 Zakharova Rassokha River, Khatanga River tributary (GIN-1456) (Andreeva, 1980)
61 3900±500 Northern Middle Siberian Upland (GIN-1182) (Bardeeva et al., 1980)
62 3910±100 Ust’-Aldan district, Yakutia (Im-362) (Kostyukevich, 1980)
63 4000±100 (Andreev et al., 1992)
64 4080±130 Kazyra River, Yenisei River head area, (MGU-260) (Endrikhmskn, 1982)
65 4280±240 Ynakhsyt River (GIN-850) (Kolpakov et al., 1980)
66 4410±200 Chadobets site, (KRIL-233) (Laukhm et al., 1980)
67 4420±50 Taimyr Peninsula (GIN-681) (Nikolskaya et al., 1980)
68 4460±50 (Andreev et al., 1992)
69 4470±200 Megin-Kangalas district, Yakutia (Im-260) (Kostyukevich, 1980)
70 Atla- 4500±40 Yana River (GIN-553) (Kolpakov et al., 1980)
71 ntic 4590±50 Molodo River (GIN-1432b) (Shofman, 1980)
72 4600±300 Megin-Kangalas district, Yakutia (Im-360) (Kostyukevich, 1980)
73 4620±50 (Andreev et al., 1992)
74 4725±190 Ust’-Aldan district, Yakutia (Im-363) (Kostyukevich, 1980)
75 4790±60 Northern Middle Siberian Upland (GIN-499) (Bardeeva et al., 1980)
76 4800±80 Molodo River (GIN-1428) (Shofman, 1980)
77 4800±60 Dulgalakh River (GIN-849) (Kolpakov et al., 1980)
78 4870±80 Omoloi River, (GIN-711) (Kolpakov et al., 1980)
79 4890±50 Yana River (GIN-554) (Kolpakov et al., 1980)
80 4920±100 Dulgalakh River (GIN-699) (Kolpakov et al., 1980)
81 4950±50 Molodo River (GIN-1432a) (Shofman, 1980)
82 5030±60 (Andreev et al., 1992)
83 5110±80 (Andreev et al., 1992)
84 5180 Taimyr Peninsula (IMSOAN-681) (Nikolskaya et al., 1980)
85 5230±70 Molodo River (GIN-1425) (Shofman, 1980)
86 5300±250 Northern Middle Siberian Upland (GIN-1184) (Bardeeva et al., 1980)
87 5320±100 Dulgalakh River (GIN-701) (Kolpakov et al., 1980)
88 5330±50 Bytantai River (GIN-546) (Kolpakov et al., 1980)
89 5480±70 (Andreev et al., 1992)
90 5500±50 Bytantai River (GIN-548) (Kolpakov et al., 1980)
91 5500±100 Taimyr Peninsula (GIN-979) (Nikolskaya et al., 1980)
92 5530±60 (Andreev et al., 1992)
93 5550±70 (Andreev et al., 1992)
94 5570±80 (Andreev et al., 1992)
95 5570±30 Bytantai River (GIN-552) (Kolpakov et al., 1980)
96 5730±200 Ishi River, Katun’ River tributary (LG-62) (Endrikhmskn, 1982)
97 5990±50 Taimyr Peninsula (GIN-1460) (Nikolskaya et al., 1980)
98 6120±70 Taimyr Peninsula (GIN-682) (Nikolskaya et al., 1980)
99 6150±60 Taimyr Peninsula (GIN-1544) (Nikolskaya et al., 1980)
100 6200±50 Undyulong, Begidzhyan, and Sobopol rivers (GIN-222) (Kolpakov et al., 1980)
101 6290±100 Irtysh River, town of Semipalatinsk (LG-40) (Endrikhmskn, 1982)
102 6390±80 (Andreev et al., 1992)
No.
103
104
105
106
107
108
109
110
111
112
113
114
115
116
117
118
119
120
121
122
123
124
125
126
127
128
129
130
131
132
133
134
135
136
137
138
139
140
141
142
143
144
145
146
147
148
149
150
151
152
153
154
155
6400±200 Northern Middle Siberian Upland (GIN-1185) (Bardeeva et al., 1980) 6670±40 Tumara River (GIN-536) (Kolpakov et al., 1980)
6695±150 Gorelyi Les site, Belaya River (Ri-50) (Endrikhmskn, 1982)
7060±100 (Andreev et al., 1992)
7210±? Severnaya Zemlya Archipelago (Bolshiyanov et al., 1995)
7270±100 Bytantai River (GIN-547) (Kolpakov et al., 1980)
7420±90 Bytantai River (GIN-549) (Kolpakov et al., 1980)
7430±230 Shsihskino archaeological monument, Lena River (Endrikhmskn, 1982)
7440±40 Taimyr Peninsula (GIN-1457) (Nikolskaya et al., 1980)
7740±70 (Andreev et al., 1992)
7780±100 (Andreev et al., 1992)
7810±150 Northern Middle Siberian Upland (GIN-500) (Bardeeva et al., 1980) 7880±120 (Andreev et al., 1992)
7950±50 (Andreev et al., 1992)
Boreal 8000±700 8030 8090 8160±20 8200±80 8220±120 8270±150 8310±70 8340±100 8340±80 8370±400 8390±40 8400±600 8444±124 8490±70 8580±50 8600±70 8600±90 8600±100 8650±200 8650±235 8730±50 8800±130 8960± 9000±150 9100±100 9120±200 9130±70
Shsihskino archaeological monument, Lena River (Endrikhmskn, 1982) Taimyr Peninsula (Nikolskaya et al., 1980)
Taimyr Peninsula (Nikolskaya et al., 1980)
Molodo River (GIN-1435) (Shofman, 1980)
Bukhuruk River (GIN-707) (Kolpakov et al., 1980)
Taimyr Peninsula (GIN-1198) (Nikolskaya et al., 1980)
Shsihskino archaeological monument, Lena River (Endrikhmskn, 1982) Taimyr Peninsula (GIN-774) (Nikolskaya et al., 1980)
Northern Middle Siberian Upland (GIN-1183) (Bardeeva et al., 1980) Dulgalakh River (GIN-853) (Kolpakov et al., 1980)
(Andreev et al., 1992)
Molodo River (GIN-1426) (Shofman, 1980)
Northern Middle Siberian Upland (GIN-522) (Bardeeva et al., 1980) Gorelyi Les site, Belaya River (Ri-51) (Endrikhmskn, 1982)
Molodo River (GIN-1431) (Shofman, 1980)
Bukhuruk River (GIN-708) (Kolpakov et al., 1980)
Taimyr Peninsula (GIN-665) (Nikolskaya et al., 1980)
Molodo River (GIN-1430) (Shofman, 1980)
Bytantai River (GIN-557) (Kolpakov et al., 1980) Khara-Bulugunnyakh (Im-262) (Kostyukevich, 1980)
Chik River, Altai (SOAN-414) (Endrikhmskn, 1982)
Dulgalakh River (GIN-700) (Kolpakov et al., 1980)
Taimyr Peninsula (GIN-820) (Nikolskaya et al., 1980)
Ust’-Belaya, Angara River (GIN-96) (Endrikhmskn, 1982)
Taimyr Peninsula (GIN-680) (Nikolskaya et al., 1980)
Northern Middle Siberian Upland (GIN-1187) (Bardeeva et al., 1980) Khara-Bulugunnyakh (Im-263) (Kostyukevich, 1980)
(Andreev et al., 1992)
Prebo- 9180±100 B. Balakhnya River, Taimyr Peninsula (GIN-791) (Nikolskaya et al., 1980)
real 9200±40 Taimyr Peninsula (GIN-679) (Nikolskaya et al., 1980)
9200±100 Tumara, Kele, Tukulan, and Khandyga rivers (GIN-528) (Kolpakov et al., 1980)
9260±70 Tumara, Kele, Tukulan, and Khandyga rivers (GIN-528) (Kolpakov et al., 1980)
9300±100 B. Rassokha River, Taimyr Peninsula (GIN-1322) (Nikolskaya et al., 1980)
9460±400 Dulgalakh River (GIN-854) (Kolpakov et al., 1980)
9700±100 Tabrata River, Yenisei River head area (MGU-199) (Endrikhmskn, 1982)
9730±50 (Andreev et al., 1992)
9800±100 Bukhuruk River (GIN-706) (Kolpakov et al., 1980)
9850±500 Ust’-Belaya, Angara River (GIN-483) (Endrikhmskn, 1982)
9990±100 (Andreev et al., 1992)
No. Stage Dating Location and references
156 10160±140 Torskaya depression, Irkut River (GIN-142) (Endrikhmskii, 1982)
157 10300±50 Ulakhan-Sakkyryk River (GIN-530) (Kolpakov et al., 1980)
158 Late 10400±600 (Andreev et al., 1992)
159 Dryas 10400±200 Markha River (GIN-912) (Shofman, 1980)
160 10480±250 B. Balakhnya River, Taimyr Peninsula (GIN-792)(Nikolskaya et al., 1980)
161 10500±130 Lena River, below the Linda River mouth (GIN-852) (Kolpakov et al., 1980)
162 10720±120 Northern Middle Siberian Upland (GIN-523) (Bardeeva et al., 1980)
163 10800±250 Tumara, Kele, Tukulan, and Khandyga rivers (GIN-529) (Kolpakov et al., 1980)
164 Alle- 10860±80 Boyarka River mouth, Taimyr Peninsula (GIN-674) (Nikolskaya et al., 1980)
165 raed 10900±500 Oshurkovo site, Selenga River (Tseithn, 1979)
166 10995±400 Koira and Vitim interstream area (IM-97) (Endrikhmskii, 1982)
167 11250±180 Khamsara River, Yenisei River head (Endrikhmskii, 1982)
168 11400±500 Makarovo-2 archaeological monument, Lena River (GIN-480b) (Endrikhmskii, 1982)
169 11540±140 Markha River (GIN-899) (Shofman, 1980)
170 11800±70 Bukhuruk River (GIN-709) (Kolpakov et al., 1980)
171 11860±280 Shsihskino archaeological monument, Lena River (GIN-480a) (Endrikhmskii, 1982)
172 11950±50 Makarovo-2 archaeological monument, Lena River (GIN-481) (Endrikhmskii, 1982)
173 12000±130 Berelekhskii occurrence site of mammoth bones (LU-149) (Arslanov et al., 1980)
174 12180±120 Kokorevo-2 site, Yenisei River (LE-770) (Endrikhmskii, 1982)
175 12230±70 Berelekhskii occurrence site of mammoth bones (LU-149) (Arslanov et al., 1980)
176 12600±150 Anui River, Altai (LG-39) (Endrikhmskii, 1982)
177 12700±150 Markha River (GIN-897) (Shofman, 1980)
178 12750±120 Eltsovka River, Altai (SOAN-575) (Endrikhmskii, 1982)
179 12750±120 Vitim River (GIN-1022) (Endrikhmskii, 1982)
180 12900±300 Oshurkovo site, Selenga River (Endrikhmskii, 1982)
181 12940±270 Kokorevo-2 site, Yenisei River (LE-526) (Endrikhmskii, 1982)
182 13300±50 Kokorevo-1 site, Yenisei River (GIN-91) (Endrikhmskii, 1982)
183 13300± Kokorevo-2 site, Yenisei River (GIN-90) (Endrikhmskii, 1982)
184 13600±120 Anui River, Altai (SOAN-69) (Endrikhmskii, 1982)
185 13700±180 North Siberian Lowland (GIN-692) (Isaeva et al., 1980)
186 13700±400 Berelekhskii occurrence site of mammoth bones (LU-149) (Arslanov et al., 1980)
187 13750±70 Lebed’ River, Turochak village, Altai (SOAN-576) (Endrikhmskii, 1982)
188 13890±200 Aya village, Katun’ River (LG-92) (Endrikhmskii, 1982)
189 14100±350 North Siberian Lowland (GIN-1452) (Isaeva et al., 1980)
190 14200±100 Yana River, Ust’-Kuiga (GIN-537) (Kolpakov et al., 1980)
191 14320±330 Kokorevo-4 site, Yenisei River (LE-496) (Endrikhmskii, 1982)
192 14500±250 Linda River, below the Ynakhstakh River mouth (GIN-851) (Kolpakov et al., 1980)
193 14540±365 Anui River, Altai (SOAN-16) (Endrikhmskii, 1982)
No. Stage Dating Location and references
194 14700±150 Kokorevo-2 site, Yenisei River (GIN-262) (Endrikhinskii, 1982)
195 14750±120 Malta site, Angara River (GIN-97) (Endrikhinskii, 1982)
196 15000±300 North Siberian Lowland (GIN-1254) (Isaeva et al., 1980)
197 15200±300 Vitim River (IM-236) (Endrikhinskii, 1982)
198 15460±320 Kokorevo-4 site, Yenisei River (LE-540) (Endrikhinskii, 1982)
199 15500±50 Yana River, Mus-Khaya (GIN-541) (Kolpakov et al., 1980)
200 15630±80 North Siberian Lowland (GIN-938) (Isaeva et al., 1980)
201 15800±60 Undyulong, Begidzhyan, and Sobopol rivers (GIN-333) (Kolpakov et al., 1980)
202 15850±680 Isha River, Altai (LG-14) (Endrikhinskii, 1982)
203 17500±100 Isha River, Altai (SOAN-746) (Endrikhinskii, 1982)
204 17590±110 Shcherbakovo village, Ob River (SOAN-443) (Endrikhinskii, 1982)
205 18500±200 Tumara River (GIN-535) (Kolpakov et al., 1980)
206 19600±500 Ust’-Aldan district, Yakutia (Kostyukevich, 1980)
207 20240±740 Isha River, Altai (LG-59) (Endrikhinskii, 1982)
208 20300±5000 Vilyui River (GIN-904) (Shofman, 1980)
209 20680±270 Ikonnikovo village, Katun’ River (SOAN-441) (Endrikhinskii, 1982)
210 20790±260 Severnaya Zemlya Archipelago (LU-1069) (Bolshiyanov et al., 1995)
211 20900±300 Afontova Gora-2 site, Krasnoyarsk area (GIN-117) (Endrikhinskii, 1982)
212 21000±300 North Siberian Lowland (GIN-962) (Andreeva, 1980)
213 21260±310 Molodo River (LU-786) (Shofman, 1980)
214 23200±1800 Oshurkovo site, Selenga River (Endrikhinskii, 1982) ionium dating
215 23750±180 Shadrintsevo village, Ob River tributary (SOAN-435) (Endrikhinskii, 1982)
216 23800±190 B. Rechka River, Ob River tributary (SOAN-154) (Endrikhinskii, 1982)
217 24100±300 Yuskeevo village, Yenisei River (GIN-308) (Endrikhinskii, 1982)
218 24120±500 Irkineeva River (SOAN-127) (Laukhm et al., 1980)
219 24240±2700 Kytmanovo village, Chumysh River, Ob River tributary (SOAN-31) (Endrikhinskii, 1982)
220 24300±220 Ulkan River (Vib-45) (Endrikhinskii, 1982)
221 24490±810 Severnaya Zemlya Archipelago (LU-665) (Bolshiyanov et al., 1995)
222 24500±320 Staroglinushka village, Ob River tributary (SOAN-430) (Endrikhinskii, 1982)
223 25300±600 Altai moraines (MGU-IOAN-65) (Endrikhinskii, 1982)
224 25800±140 Pavlovshchina village, Yenisei River (GIN-310) (Endrikhinskii, 1982)
225 25900±340 Biya River (SOAN-52) (Endrikhinskii, 1982)
226 25970±180 B. Rechka River, Ob River tributary (SOAN-1257) (Endrikhinskii, 1982)
227 26030±810 Severnaya Zemlya Archipelago (LU-1143) (Bolshiyanov et al., 1995)
228 26090±640 Severnaya Zemlya Archipelago (LU-1142) (Bolshiyanov et al., 1995)
229 26200±620 Biya River (SOAN-51) (Endrikhinskii, 1982)
230 26300±900 Novonazimovo village, Yenisei River (LG-19) (Endrikhinskii, 1982)
231 26600±1000 B. Balakhnya River, North Siberian Lowland (GIN-999) (Andreeva, 1980)
232 26700±210 Shadrintsevo village, Ob River tributary (SOAN-434) (Endrikhinskii, 1982)
233 26700±700 B. Balakhnya River, North Siberian Lowland (GIN-999) (Andreeva, 1980)
234 27000±700 Zakharova Rassokha River, Khatanga River tributary (GIN-1454) (Andreeva, 1980)
235 27100±200 Molodo River (GIN-1433) (Shofman, 1980)
78
No.
236
237
238
239
240
241
242
243
244
245
246
247
248
249
250
251
252
253
254
255
256
257
258
259
260
261
262
263
264
265
266
267
268
269
270
271
272
273
274
275
276
277
278
279
280
281
27200±700 North Siberian Lowland (GIN-1454) (Andreeva, 1980)
28000±500 Tumara, Kele, Tukulan, and Khandyga rivers (GIN-533)
(Kolpakov et al., 1980)
28050±310 Pogorelka village, Ob River tributary (SOAN-1257) (Endrikhmskn, 1982) 28200±440 Vatutina Promontory Severnaya Zemlya Archipelago (LU-613)
(Bolshiyanov et al., 1995)
29500±250 Undyulong, Begidzhyan, and Sobopol rivers (GIN-345)
(Kolpakov et al., 1980)
29670±230 Irkineeva River (SOAN-128) (Laukhm et al., 1980)
29700±1000 North Siberian Lowland (GIN-693) (Andreeva, 1980)
30100±150 Ust’-Kova, Angara River tributary (GIN-1741) (Laukhm et al., 1980)
30400±300 Undyulong, Begidzhyan, and Sobopol rivers (GIN-224) (Kolpakov et al., 1980)
30600±500 Varvarina Gora site (SO AN-850) (Kind, 1974)
31000±750 North Siberian Lowland (GIN-752b) (Isaeva et al., 1980)
31450±440 Severnaya Zemlya Archipelago (LU-630) (Bolshiyanov et al., 1995)
31500±750 North Siberian Lowland (MGU-486) (Isaeva et al., 1980)
31800±400 B. Balakhnya River, North Siberian Lowland (MGU-486)
(Andreeva, 1980)
32700±2000 North Siberian Lowland (GIN-1550) (Andreeva, 1980)
32800±2000 B. Balakhnya River, North Siberian Lowland (GIN-1000)
(Andreeva, 1980)
33300±400 North Siberian Lowland (GIN-752b) (Isaeva et al., 1980)
33400±780 Irkineeva River (SO AN-129) (Laukhm et al., 1980)
33450±550 Kargopolovo village, Ob River (SOAN-744) (Endrikhmskn, 1982)
33600±700 Undyulong, Begidzhyan, and Sobopol rivers (GIN-339) (Kolpakov et al., 1980)
33950±400 Bobkovo village, Alei River, Ob River tributary (SOAN-446)
(Endrikhmskn, 1982)
34015±1515 Severnaya Zemlya Archipelago (Upsala-1285) (Bolshiyanov et al., 1995)
34650±2100 B. Yeniseiskoe village (SOAN-161) (Endrikhmskn, 1982)
34860±2100 Tolbaga village, Khilok River (SOAN-1522) (Endrikhmskn, 1982)
35100±1000 Balakhnya River, North Siberian Lowland (GIN-1458)
(Andreeva, 1980)
35110±1480 Severnaya Zemlya Archipelago (LU-1356) (Bolshiyanov et al., 1995)
35350±470 Malyshevo village, Ob River (SOAN-1633) (Endrikhmskn, 1982)
35400±700 Novosurtaevka village, Katun’ River (SOAN-747) (Endrikhmskn, 1982)
35400±2500 Beloyarskoe village, Kan River (MGU-IOAN-158) (Endrikhmskn, 1982)
35530±2310 Severnaya Zemlya Archipelago (Upsala-1795) (Bolshiyanov et al., 1995)
35800±1700 Northern Middle Siberian Upland (GIN-493) (Bardeeva et al., 1980)
35830±630 Terekhtyakh mammoth, Indigirka River basin (LU-504) (Arslanov et al., 1980)
36000 Vilyui River (GIN-890) (Shofman, 1980)
36100±200 Molodo River (GIN-1427) (Shofman, 1980)
36200±1000 North Siberian Lowland (MGU-492) (Isaeva et al., 1980)
36420±700 North Siberian Lowland (SOAN-1075) (Andreeva, 1980)
37300±1675 Severnaya Zemlya Archipelago (Upsala-1385) (Bolshiyanov et al., 1995)
37340±660 B. Rechka River, Ob River tributary (SOAN-1258) (Endrikhmskn, 1982)
37500±1000 North Siberian Lowland (SOAN-834) (Andreeva, 1980)
37600±800 Vilyui River (GIN-1103) (Shofman, 1980)
37900±700 Undyulong, Begidzhyan, and Sobopol rivers (GIN-343) (Kolpakov et al., 1980)
37950±1150 Irkineeva River (KSM-10) (Laukhm et al., 1980)
38000±? Severnaya Zemlya Archipelago (Bolshiyanov et al., 1995)
38200±2500 Beloyarskoe village, Kan River (MGU-IOAN-153) (Endrikhmskn, 1982)
38400±800 Vilyui River (GIN-1104) (Shofman, 1980)
38400±800 Lena River, below the Aldan River mouth (GIN-545) (Kolpakov et al., 1980)
No.
282
283
284
285
286
287
288
289
290
291
292
293
294
295
296
297
298
299
300
301
302
303
304
305
306
307
308
309
310
311
312
313
314
315
316
317
318
319
320
321
322
323
324
325
326
327
38500±1000
38590±1120
38590±770
38800±?
38800±1600
38850±2200
39000±1000
39000±2000
39350±760
39420±490
39500±2000
39500±500
39570±870
39600±1200
39700±700
39900±1500
40310±1230
40350±880
40450±1000
40600±800
40600±1900
40900±1000
41200±3000
41200±2000
41240±?
41300±1500
41600±1300
41750±1290
42000±1500
42000±1500
42600±1500
42800±1300
42920±1240
43000±1000
43100±1200
43100±1800
43100±1850
43200±1100
43500±1000 44000±1600 44000±1500 Karga 44500±1000
45500±1500
45560±1870
45900±1570
46100±?
Vilyui River (GIN-1100) (Shofman, 1980)
Selirikan horse, Balakhan River, Indigirka River basin (LU-506)
(Arslanov et at, 1980)
Magadan young mammoth (LU-718V) (Arslanov et at, 1980) Kargopolovo village, Ob River (SOAN-25) (Endrikhmskn, 1982)
Yana River, Mus-Khaya (GIN-500) (Kolpakov et al, 1980)
Irkineeva River (SOAN-130) (Laukhm et al, 1980)
Baty-Sala River, North Siberian Lowland (GIN-1441)
(Andreeva, 1980)
Molodo River (GIN-1435) (Shofman, 1980)
Shcherbakovo village, Ob River (SOAN-AAb) (Endrikhmskn, 1982) Severnaya Zemlya Archipelago (LU-558) (Bolshiyanov et al., 1995) Lake Taimyr, North Siberian Lowland (GIN-794)
(Andreeva, 1980)
Markha River (GIN-906) (Shofman, 1980)
Magadan young mammoth (LU-718A) (Arslanov et al., 1980) Novosurtaevka village, Katun’ River (SOAN-748) (Endrikhmskn, 1982) North Siberian Lowland (GIN-735) (Isaeva et al., 1980)
North Siberian Lowland (GIN-784) (Andreeva, 1980)
Glacier-dammed features, Allakh-Yun’ River,
Priverkhoyan’e area (LU-602) (Zamoruev, 1979)
Mammoth, Shandrin River, Yakutia (LU-595) (Arslanov et al., 1980) Malyshevo village, Ob River (SOAN-1632) (Endrikhmskn, 1982)
North Siberian Lowland (GIN-1150) (Isaeva et al., 1980)
Molodo River (GIN-1429) (Shofman, 1980)
Vilyui River (GIN-1101) (Shofman, 1980)
B. Yeniseiskoe village (SOAN-751) (Endrikhmskn, 1982)
North Siberian Lowland (GIN-1534) (Isaeva et al., 1980)
Severnaya Zemlya Archipelago (LU-1325) (Bolshiyanov et al., 1995) Yana River, Mus-Khaya (GIN-538) (Kolpakov et al., 1980)
Irkineeva River (KSM-11) (Laukhm et al., 1980)
Mammoth, Shandrin River, Yakutia (LU-595) (Arslanov et al., 1980) Vilyui River (GIN-891) (Shofman, 1980)
Vilyui River (GIN-1106) (Shofman, 1980)
Boyarka River North Siberian Lowland (GIN-673) (Andreeva, 1980) Malaya River, North Siberian Lowland (GIN-1530) (Andreeva, 1980) Severnaya Zemlya Archipelago (LU-1672) (Bolshiyanov et al., 1995) Severnaya Zemlya Archipelago (LU-592) (Bolshiyanov et al., 1995)
B. Romanikha River, North Siberian Lowland (GIN-1010)
(Andreeva, 1980)
Markha River (GIN-896) (Shofman, 1980)
Vacha River (SOAN-406) (Tishchenko, 1982)
Tumara, Kele, Tukulan, and Khandyga rivers (GIN-525)
(Kolpakov et al., 1980)
Yana River, above Ust’-Kuiga (GIN-524) (Kolpakov et al., 1980)
Vilyui River (GIN-1105) (Shofman, 1980)
Ulakhan-Sakkyryk River (GIN-704) (Kolpakov et al., 1980)
Balakhnya River, North Siberian Lowland (GIN-1004)
(Andreeva, 1980)
Tumara, Kele, Tukulan, and Khandyga rivers (Kolpakov et al., 1980) Severnaya Zemlya Archipelago (LU-1278) (Bolshiyanov et al., 1995) Severnaya Zemlya Archipelago (LU-1121) (Bolshiyanov et al., 1995) Severnaya Zemlya Archipelago (LU-1075) (Bolshiyanov et al., 1995)
No. Stage Dating Location and references
328 46200±2000 Bata-Sala River, North Siberian Lowland (GIN-1152) (Andreeva, 1980)
329 46550±1350 Severnaya Zemlya Archipelago (LU-1074) (Bolshiyanov et al., 1995)
330 46600±1200 Lake Taimyr, North Siberian Lowland (GIN-1324) (Andreeva, 1980)
331 47000±1000 Irkineeva River (KSM-41) (Laukhm et al, 1980)
332 47600±1600 Aldan River (GIN-845) (Kolpakov et al., 1980)
333 48150±3500 Vacha River (SOAN-405) (Tishchenko, 1982)
334 48700 Vilyui River (GIN-1102) (Shofman, 1980)
335 48800±2000 Ulakhan-Sakkyryk River (GIN-705) (Kolpakov et al., 1980)
336 50000±2000 Markha River (GIN-893) (Shofman, 1980)
337 50000 Vilyui River (GIN-892) (Shofman, 1980)
338 51470±? Severnaya Zemlya Archipelago (LU-1080) (Bolshiyanov et al., 1995)
339 51740±1500 Severnaya Zemlya Archipelago (LU-569) (Bolshiyanov et al. 1995)
340 52200±860 Severnaya Zemlya Archipelago (LU-570) (Bolshiyanov et al. 1995)
341 54040±? Severnaya Zemlya Archipelago (LU-590) (Bolshiyanov et al. 1995)
342 54790±? Severnaya Zemlya Archipelago (LU-593) (Bolshiyanov et al. 1995)
343 55230 Severnaya Zemlya Archipelago (LU-591) (Bolshiyanov et al. 1995)
344 55900±2200 Severnaya Zemlya Archipelago (LU-571) (Bolshiyanov et al. 1995)
Table 3. Occurrence calendar of ancient people sites in southern Siberia
No. Pleistocene stages Historical epochs Dating Location and references
1 Late Holocene 2130±145 Berloga site, Priolkhon’e Island (Goryunova et al., 1996)
2 Iron Age 2230±100 Chadobets site, soil (KRIL-231) (Laukhm et al., 1980)
3 3200 2990±120 Chadobets site, soil (KRIL-232) (Laukhm et al., 1980)
4 Bronze 3440±20 Tyshkino site, Priolkhon’e Island (SOAN-2511) (Goryunova et al., 1996)
5 Age 3500 2500 3525±25 Tyshkino site, Priolkhon’e Island (SOAN-2512) (Goryunova et al., 1996)
6 3620±50 Ulan-Khada archaeological monument, Priolkhon’e Island (GIN-4875) (Goryunova et al., 1996)
7 3660±60 Ulan-Khada archaeological monument, Priolkhon’e Island (LE-883) (Goryunova et al., 1996)
8 3660±20 («-2513) Tyshkino site, Priolkhon’e Island (SOAN-2513)(Goryunova et al., 1996)
9 3710±100 Ulan-Khada archaeological monument, Priolkhon’e Island (LE-1279) (Goryunova et al., 1996)
10 3780±40 Tyshkino site, Priolkhon’e Island (GIN-4880) (Goryunova et al., 1996)
11 3800±100 Neolithic and Mesolithic paleosol cultural layer, Olkhon and Priolkhon’e Islands (LE-1277) (Mats, 1987)
12 4000±50 Ulan-Khada archaeological monument, Priolkhon’e Island (GIN-4876) (Goryunova et al., 1996)
13 4030±115 Ulan-Khada archaeological monument, Priolkhon’e Island (SOAN-3335) (Goryunova et al., 1996)
14 4060±80 Ulan-Khada archaeological monument, Priolkhon’e Island (GIN-4877) (Goryunova et al., 1996)
No. Pleistocene stages Historical epochs Dating Location and references
origin of cattle-breeding 5000 years ago
15 Late 4150±80 Ulan-Khada archaeological monument, Priolkhon’e (LE-1280) (Goryunova et al., 1996)
16 Middle Holocene 4220±120 Neolithic and Mesolithic paleosol cultural layer, Olkhon and Priolkhon’e Islands (LE-1278) (Mats, 1987)
17 4410±200 Chadobets site, soil (KRIL-233) (Laukhm et al., 1980)
18 4430±15 Ityrkhei-V, VI, archaeological monument, Priolkhon’e Island (Vorob’eva et al., 1992)
19 4470±65 Neolithic culture on the surface of the 1st terrace, conclusion of the 1st terrace formation, Boguchanskaya Bay (SOAN-830) (Mats, 1987)
20 4485±45 Ityrkhei site, Priolkhon’e Island (SOAN-1585) (Goryunova et al., 1996)
21 4500±100 Ulan-Khada archaeological monument, Priolkhon’e Island (Vorob’eva et al., 1992)
22 4560±100 Neolithic and Mesolithic paleosol cultural layer, Olkhon and Priolkhon’e Islands (LE-1282) (Mats, 1987)
23 4600±60 Kazachka IV site (Vorob’eva et al., 1992)
24 4740±155 Ityrkhei site, Priolkhon’e Island (SOAN-3342) (Goryunova et al., 1996)
25 Eneolithic (Copper- 5430±120 Gorelyi Les site (Vorob’eva et al., 1992)
26 Late Stone Age) 5495±125 Ulan-Khada archaeological monument, Priolkhon’e
Middle 6000 5000 Island (SOAN-3336) (Goryunova et al., 1996)
27 Holocene Neolithic in the Baikal 5680±60 Ityrkhei site, Priolkhon’e Island (SOAN-3341) (Goryunova et al., 1996)
28 region 6000 3200 5700±200 Ityrkhei site, Priolkhon’e Island (GIN-4881) (Goryunova et al., 1996)
29 6525±100 Berloga site, Priolkhon’e Island (SOAN-3169) (Goryunova et al., 1996)
30 6650±200 Kazachka VI archaeological monument (Vorob’eva et al., 1992)
31 6695±150 Gorelyi Les VI site (Vorob’eva et al., 1992)
32 Early Middle Holocene 6850±210 Kazachka VIII archaeological monument (Vorob’eva et al., 1992)
33 6996±150 Gorelyi Les VI archaeological monument (Vorob’eva et al., 1992)
34 7300±290 Neolithic and Mesolithic paleosol cultural layer, Olkhon and Priolkhon’e Islands (IMSOAN-402) (Mats, 1987)
35 7430±230 Shishkino archaeological monument, Lena River (Endrikhinskii, 1982)
36 7620±900 Sagan-Nuge site, Priolkhon’e Island (SOAN-3056) (Goryunova et al., 1996)
37 8000±150 Kazachka XII archaeological monument (Vorob’eva et al., 1992)
38 8000±700 Shishkino site, Lena River, 1st above-floodplain terrace (Kind et al., cited in Aksenov et al., 1975)
No. Pleistocene stages Historical epochs Dating Location and references
39 8010±100 Ityrkhei site, Priolkhon’e Island (GIN-4882) (Goryunova et at, 1996)
40 8100±150 Kazachka XI archaeological monument (Vorob’eva et al., 1992)
41 8270±150 Shishkino archaeological monument, Lena River (GIN-303) (Endrikhmskn, 1982)
42 8270±150 Berloga site, Priolkhon’e Island (SOAN-3340) (Goryunova et al., 1996)
43 8300±250 Kazachka XI archaeological monument (.Aksenov et al., 1992)
44 8444±124 Mesolithic Gorelyi Les site, southern Angara area, elevated floodplain (Medvedev et al., 1975)
45 Early Neolithic 8720±210 Ityrkhei site, Priolkhon’e Island
Holocene 10000- (SOAN-3171) (Goryunova et al., 1996)
46 -8000 8855±300 Mesolithic Gorelyi Les site, southern Angara area, elevated floodplain (KRIL-234) (Medvedev et al., 1975)
47 8960±60 1st above-floodplain terrace alluvium of the Angara River, Belaya River mouth area (GIN-96) (Tsettltn, 1975)
48 9105±70 Berloga site, Priolkhon’e Island (SOAN-3059) (Goryunova et al., 1996)
49 9360±95 Sagan-Nuge site, Priolkhon’e Island (SOAN-3337) (Goryunova et al., 1996)
50 9815±80 Sagan-Nuge site, Priolkhon’e Island (SOAN-3058) (Goryunova et al., 1996)
51 9850±500 1st above-floodplain terrace alluvium of the Angara River, Belaya River mouth area (GIN-483) ( Tsettltn, 1975)
52 10145±290 Berloga site, Priolkhon’e Island (SOAN-3060) (Goryunova et al., 1996)
53 10290±40 Sagan-Nuge site, Priolkhon’e Island (SOAN-3057) (Goryunova et al., 1996)
54 10900±500 Oshurkovo site, Selenga River (Endrtkhtnsktt, 1982)
55 Oldest Holocene Mesolithic 11400±500 Makarovo II archaeological monument, Lena River head area (GIN-480b) (Kind et al., 1972, cited in Aksenov et al., 1975)
56 12000- -10000 11860±200 Makarovo II archaeological monument, Lena River head area (GIN-480a) (Kind et al., 1972, cited in Aksenov et al., 1975)
57 11930±230 Ust ’-Belaya XIV archaeological monument (Aksenov et al., 1992)
58 11950±50 Makarovo II archaeological monument, Lena River head area (GIN-481) (Kind et al., 1972, cited in Aksenov et al., 1975)
59 12180±120 Kokorevo-2 site (LE-770), Yenisei River (Endrtkhtnsktt, 1982)
60 12570±180 Mesolithic Verkholenskaya Gora site, alluvium of the 3rd above-floodplain terrace (MO-441) (Medvedev et al., 1975)
61 12900±300 Oshurkovo site, Selenga River (Endrtkhtnsktt, 1982)
No. Pleistocene Historical Dating Location and references
stages epochs
62 12940±270 Kokorevo-2 site, Yenisei River (LE-526) (Endrikhmskn, 1982)
63 13300±50 Kokorevo-1 site, Yenisei River (GIN-91) (Endrikhmskn, 1982)
64 13300±? Kokorevo-2 site, Yenisei River (GIN-90) (Endrikhmskn, 1982)
65 14320±330 Kokorevo-4 site, Yenisei River (LE-496) (Endrikhmskn, 1982)
66 14700±150 Kokorevo-2 site, Yenisei River (GIN-262) (Endrikhmskn, 1982)
67 14720±190 Malta archaeological monument (GIN-8476) (Medvedev et al, 1996)
68 14750±120 Malta archaeological monument (GIN-97) (Medvedev et al, 1996)
69 15200±1250 Kurla archaeological monument (SOAN-1396) (Medvedev et al, 1990)
70 15460±320 Kokorevo-4 site, Yenisei River (LE-540) (Medvedev et al, 1990)
71 Late Pleistocene 19100±100 Krasnyi Yar archaeological monument (GIN-5530) (Medvedev et al, 1990)
72 Samar ovo Glaciation 19900±800 Malta archaeological monument (GIN-7705) (Medvedev et al, 1996)
73 20340±320 Malta archaeological monument (OkhA-6192) (Medvedev et al., 1996)
74 20700±150 Malta archaeological monument (GIN-7709) (Medvedev et al, 1996)
75 20800±140 Malta archaeological monument (GIN-7710) (Medvedev et al, 1996)
76 20800±200 Malta archaeological monument (GIN-4367) (Medvedev et al, 1996)
77 20900±300 Afontova Gora-2 archaeological monument, Krasnoyarsk area (GIN-117) (Endrikhmskn, 1982)
78 20900±200 Malta archaeological monument (GIN-4367) (Medvedev et al, 1996)
79 21000±140 Malta archaeological monument (GIN-7706) (Medvedev et al, 1996)
80 21100±110 Malta archaeological monument (GIN-7703) (Medvedev et al, 1996)
81 21190±100 Buret’ archaeological monument, Angara River (Medvedev et al, 1990)
82 21260±240 Itegeiskii Log archaeological monument (LE-1590)(Mecfoe<iei> et al, 1990)
83 21300±110 Malta archaeological monument (GIN-7704) (Medvedev et al, 1996)
84 21300±300 Malta archaeological monument (GIN-7702) (Medvedev et al, 1996)
85 21340±340 Malta archaeological monument (OkhA-6193) (Medvedev et al, 1996)
86 21600±170 Malta archaeological monument (GIN-8475) (Medvedev et al, 1996)
No. Pleistocene stages Historical epochs Dating Location and references
87 21600±200 Malta archaeological monument (GIN-7708) (Medvedev et al., 1996)
88 21700±160 Malta archaeological monument (OkhA-6191) (Medvedev et al., 1996)
89 Upper Paleolithic 12000- -40000 23000±5000 Malta archaeological monument, alluvium of the 3rd above-floodplain terrace, Belaya River, ionium dating (Cherdyntsev, 1961, cited in [Tsettltn, 1975; Medvedev et al., 1990])
90 23200±1800 Oshurkovo site, Selenga River (Endrikhmskn, 1982)
91 23508±250 Igeteiskii Log archaeological monument (LE-1592) (Medvedev et al., 1990)
92 Late Pleistocene 23700±100 Igetei archaeological monument (IM SOAN-405) (Medvedev et al., 1990)
93 Karginsky Inter- 23760±1100 Upper Paleolithic Igeteiskii Log archaeological monument (IM SOAN-405) (Medvedev et ai, 1990)
94 glacial 23780±600 Igetei archaeological monument (SOAN-1681) (Medvedev et al., 1990)
95 24060±570 Kurla archaeological monument, northern Baikal (SOAN-1397) Medvedev et al., 1990)
96 24400±400 Itegeiskii Log archaeological monument (GIN-5327) (Medvedev et al, 1990)
97 25760±260 Malta archaeological monument (OkhA-6190) (Medvedev et al, 1996)
98 29700±500 Voennyi Gospital archaeological monument, spit between the Angara and Ushakovka Rivers (GIN-4440) (Medvedev et al, 1990)
99 41100±1500 Malta archaeological monument (GIN-7707) (Medvedev et al, 1996)
100 43100±2400 Malta archaeological monument (OkhA-6189) (Medvedev et al, 1996)
53-36 ka, Kazantsevo time; 50-42 ka, early Karginsky time; 42-33 ka, Malokhetsky time; 33-24 ka, late Karginsky time; 17-10 ka, Sartan time
References
Aksenov, M.P., Lypsha, V.A., and Shun’kov, M.V., Complex of pre-Neolithic occurrences near the Kistenevo village, upper Lena River, in Ancient History of Peoples in Southern East Siberia, vol. 3, pp. 81-114, Irkutsk, 1975 (in Russian).
Andreev, A.A., Klimanov, V.A., and Sulerzhitskii, L.D., History of vegetation and climate in central Yakutia over the past 11000 years, in Geochronology of the Quaternary, pp. 113-117, Moscow, Nauka, 1992 (in Russian).
Andreeva, S.M., North Siberian lowland at the Kargin-sky time (50-24 ka). Paleogeography and radiocarbon chronology, in Geochronology of the Quaternary, pp. 183191, Moscow, Nauka, 1992 (in Russian).
Arslanov, Kh.A., Vereshchagin, N.K., Lyadov, V.V., and Ukraintsev, V.V., On the chronology of the Karginsky Interglacial and reconstruction of Siberian landscapes from
the study of mammoth corpses and their “satellites”, in Geochronology of the Quaternary, pp. 208-209, Moscow, Nauka, 1992 (in Russian).
Bardeeva, M.A., Isaeva, L.L., Andreeva, S.M., et al., Stratigraphy, geochronology, and paleogeography of the Late Pleistocene and Holocene in the northern Central Siberian Upland, in Geochronology of the Quaternary, pp. 191-197, Moscow, Nauka, 1992 (in Russian).
Bezrukova, E.V., Vegetation and climate in the Baikal region at the postglacial and Holocene time, and. Sc. Dissertation, Novosibirsk, 1996 (in Russian).
Bolshiyanov, D.Yu. and Makeev, V.M., Severnaya Zemlya Archipelago: Glaciation and the History of the Natural Environment, Saint Petersburg, Gidrometeoizdat, 1995 (in Russian).
Chichagov, V.P., Radiocarbon constraints on natural and anthropogenic factors contributing to the acceleration of contemporary geodynamic processes, in Geochronology of
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