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IGCP 610 First Plenary Meeting and Field Trip, Tbilisi, Georgia, 12-19 October 2013

ORAL

Paleogeography of the Caspian late Pleistocene: New data.

Yanina T.A.

1

, Sorokin V.M.

1

, Bezrodnykh Yu.P.

2

,

Romanyuk B.F.

2

1

M.V. Lomonosov Moscow State University, Moscow, 119992, Russia

2

didacna@mail.ru

АО «Мorinzhgeologiya», Riga, Latvia

paleo@inbox.ru

Keywords: Caspian Sea, late Pleistocene, cores, transgressive deposits, regressive sediments, radiocarbon dating, paleogeography

The event scheme of the Caspian Late Pleistocene includes Late Khazar (Late Khazar and Girkan transgressive stages) and Khvalynian (Early Khvalynian and Late Khvalynian transgressive stages) transgressive epochs, separated by the Atel regression. Many questions of a paleogeography of these transgressive and regressive events (quantity of stages, age, environmental conditions, correlation with events in the neighboring territories and with climatic events) are debatable. The main part of a material on a problem is received as a result of researches on the coasts of the Caspian

Sea. Therefore undoubted interest in researchers is caused by drilling materials on the bottom of the

Caspian Sea. We studied the cores of the wells (sequences of the boreholes) up to 100 m in depth drilled during engineering-geological researches in the Northern Caspian Sea. They opened thickness of late Pleistocene deposits with difficult construction. Studying of the structure of the section and spatial correlation of lithological-stratigraphical thicknesses are executed by means of seismoacoustic profiling and static sounding. The sediments of the cores are studied by lithological, malakofaunistic and geochronological methods. Among mollusks we mainly focused on the brackish water species of genus

Didacna

Eichw. Members of this genus are endemic and index species for the Caspian Sea. This genus is known for its high evolutionary rates at the species and subspecies levels, which highlight its significance for the stratification of the marine Pleistocene of the Caspian and for paleogeographic reconstructions of the Caspian basins.

The Late Khazar transgression developed in two independent stages, separated with a regression.

Sea-level of the earlier Late Khazar basin, according to sediment spatial distribution, did not exceed -10m, and its area was much bigger (more?) than the modern Caspian. Malacologic fauna represent a faunal assemblage with crassoidal

Didacna

and characteristic species

D. nalivkini

and

D. surachanica

. Its distinguishing feature is large dimensions and massiveness of shells, especially common for southern parts of the Caspian. Common gigantism of shells, high carbonate content in the sediment and presence of oolites indicated the warm climate of the Late Khazar. Warm waters of the basin, obviously, had higher salinity than in the modern Caspian: between 10-12‰ for the northern and up to 14-15‰ for the southern Caspian Sea (Yanina, 2012). Early Late Khazar transgression stage was followed by a regression. It was evidenced by hiatuses in marine sedimentation

(Dagestan), and wash-outs and soil formation (Volga River valley) (Svitoch, Yanina, 1997).

Traces of the second transgressive Late Khazar stage are not preserved at the Caspian coasts. Based on drill sites materials from the north-western part of the Caspian region, G.I. Popov (1983) reconstructed a freshened brackish water basin. He defined it as an independent Girkan transgression of the Caspian, which took place after the Late Khazar transgression and was separated from the

Khvalynian transgression by the Atel regression. The basin was inhabited by “Khvalynian-like” fauna, traces of which have not been recorded elsewhere. A number of researchers strongly objected to this concept.

The structure of the cores studied by us showed that between two regressive thicknesses (Chernoyarsk and Atel) two thicknesses of the marine deposits are located. The lower part of the late

Khazar deposits is most fully presented on northern structures. Sandy sediments in the basis of the studied cuts (sequences) are characterized by domination of fresh-water species (

Corbicula flumiwww.avalon-institute.org/IGCP

IGCP 610 First Plenary Meeting and Field Trip, Tbilisi, Georgia, 12-19 October 2013 nalis, Lymnaea stagnalis, Valvata sp

.) with impurity of the slightly brackish water species. They characterize the shallow warm-water almost fresh-water basin existing on the place of modern central part of the Northern Caspian Sea. Sediments of higher intervals contain the malakofaunistic complex, which feature - a combination of two thermophilic species belonging to different types of fauna:

Didacna nalivkini

and

Corbicula fluminalis,

and also rare

D. surachanica, D. vulgaris

,

D. pallаsi

, with obviousness testifying to late Khazar age of the complex. It characterizes the brackish water shallow warm-water basin with inflow of fresh waters. The described layers reflect different phases of development of the late Khazar transgression.

The following stage of development of the Caspian Sea is presented by sandy-clay deposits. Feature of its faunistic complex is the abundance of

D. subcatillus,

the occurrence of

D. cristata

and species of Khazar type

D. pallasi, D. shuraosenica, D. subcrassa

. According to materials of G.I.

Popov (1983),

D. subcatillus

in combination with

D. cristata

are the "face" for the Girkan fauna.

Probably, the described by us thickness belong to Girkan transgression. The radio-carbon datings

(> 40 thousand years ago) can testify to it. The conclusion about the taxonomical status of this transgression and its age can be made only after dating of this thickness, and also spreading it late

Khazar thickness, by methods, which opportunities extend for the end of middle Pleistocene and the beginning of late Pleistocene.

Beginning of the late Pleistocene was characterized by the warm interglacial epoch (MIS 5), the

Mikulino interglaciation on the Russian Plain. Late Khazar and Girkan transgressions corresponded to this warm epoch.

The end of the Khazar stage of the Caspian development was marked by the deep Atel regression.

During this time vast areas of the Caspian shelf were exposed. Out of all continental formations of regressive Caspian epochs, sediments of this one are the most widely spread and are found at all

Caspian coasts (Svitoch, Yanina, 1997). Atel regressive sediments are well expressed in the cores.

They transformed by subaeral environment, deposits include the fresh-water mollusks and the vegetable remains. In the Lower Volga region in the base of the regressive layer there are Akhtuba deposits, first distinguished by G.I. Goretskiy (1958) and referred to as a periglacial formation. They represent a perfect marking horizon in the Lower Volga sections, often with sharp wedges penetrating the underlying sediments. These wedges and winterkill fractures in the base of Akhtuba sands are syngenetic to them, and represent the convincing proof of the severe climatic conditions at the time of deposition and permafrost development. It is obvious, that upon approaching the cooling maximum (MIS 4, early Valday glaciations on the Russian plain), the transgressive development of the Caspian was disrupted by the Atel regression under cold and dry climate.

The Atel regression was followed by the Khvalynian transgression with the most significant sealevel rise in the late Pleistocene history of the Caspian. Unlike earlier transgressions, traces of

Khvalynian Sea development are found at all Caspian coasts. The maximum sea-level can be easily traced by the distinct marked relief found with rare exceptions, at levels of 46-50 m absolute scale throughout the entire perimeter of the paleobasin. Almost all researchers who studied the Caspian history agree that there are two Khvalynian transgressions – early and late Khvalynian, separated by the Enotaevka regression.

Drilling material and datings, obtained from shells and organic matter from sediment cores, are of great interest. The Khvalynian section on the bigger square of the Northern Caspian Sea begins by a layer of a coarse-grained marine sediments with faunal material, among them the community of

Didacna subcatillus

is predominated.

14

C age is from 28,5 to 31,5 ky; the calibrated dates are from

33,5 to 36,5 ky. Thickness of deep-water clay deposits with inclusion of typical Khvalynian fauna of

Didacna protracta

,

D. parallella

blocks it. According to structure of the cores and properties of malakofauna (

Didacna protracta submedia

,

Dreissena rostriformis compressa

), this thickness answers the most deep-water Khvalynian basin. Dating of this interval by

14

C method gave the age about 27 ky ago (the calibrated dates about 32 ky ago) (Bezrodnykh et al., 2004, 2013). Evidently, the first transgressive stage of the Khvalynian transgression took place during the warming of the

MIS 3, in the Valday interstadial.

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IGCP 610 First Plenary Meeting and Field Trip, Tbilisi, Georgia, 12-19 October 2013

Above it in the number of boreholes (mainly in the southern part of the Northern Caspian Sea) accumulation of sandy and dusty sediments was noted. Obviously, they correspond to fall of level of the Khvalynian Sea. Age interval of this event was from 22 to 19 thousand years ago. Apparently, this fall of level answers the last glacial maximum (MIS 2, late Valday glaciation). In northern areas of the Caspian Sea this stage is fixed in the cores structure by washouts.

This pack of deposits is blocked in the southern part by a sandy-clay sediments with thick up to 2 m; clay deposits of brown coloring with thickness up to 5 m lie on them with washout. This clay thickness is marked in the all cores. It is characterized

by Didacna parallella

,

D. protracta

,

D. ebersini

,

D. praetrigonoides.

According to

14

C datings its age interval is 17645-16075. The authors have no consensus about paleogeographic treatment (early or late Khvalynian transgression) of this thickness. Transgression development occurred during the degradation of the late Valday glaciation.

The Khvalynian cycle of deposits comes to the end with marine-deltaic sediments in the northern part of the Northern Caspian Sea and sandy sediments in its southern part. On the deposits, answering to Mangyshlak regression (sapropel and peat), the

14

C dating between 8,8-9,6 ky ago (the calibrated dates 9,9-10,9 ky) are received. It corresponded to the climate continentalization of the early

Holocene.

Drilling materials on the water area (bottom) of the Caspian Sea show, what not all events of the late Pleistocene history of the Caspian Sea are reflected in the deposits of the coasts. Actual problem is correlation of the Caspian thicknesses opened by boreholes, and deposits exposed in the coastal sections. Only this way will lead us to the fullest interpretation of the Pleistocene history of the Caspian Sea.

The work is partly performed with financial support of RFBR (Grant 13-05-00242).

References

Bezrodnykh, Yu.P., Romanyuk, B.F., Deliya, S.V., Magomedov R.D., Parunin, O.B., Sorokin,

V.M., Babak, E.V. 2004. Biostratigraphy, structure of the upper Quaternary deposits and some paleogeographic features of the North Caspian region.

Stratigraphy and Geological

Correlation

, 12 (1): 102-111.

Bezrodnykh, Yu.P., Romanyuk, B.F., Deliya, S.V., Sorokin, V.M., Yanina T.A., Arslanov Kh.A.

2013. Novye daanye po biostratigrafii I paleogeografii kaspiyskogo pozdnego pleistotsena

[New data on the biostratigraphy and paleogeography of the Caspian late Pleistocene]. In:

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Don, Southern branch of the RAS. (in Russian).

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22: 26-44. (in Russian).

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Caspian Straits].

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Svitoch, A.A., Yanina, T.A. 1997.

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www.avalon-institute.org/IGCP

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