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УДК 551.7+903.4] (262.5)
Glebov A.Yu.
TWO MAIN LATE PLEISTOCENE - HOLOCENE EVENTS IN THE BLACK SEA
The refined seismic stratigraphic model of the structure and formation of the Upper Pleistocene-Holocene section of the Black Sea is offered for discussion. There are two major events that are ubiquitously recorded in the section: a large-scale regressive-transgressive cycle of Post-Karangatian-Neoeuxinian age and a regressive transgressive cycle at the Pleistocene Holocene boundary.
At this stage, we would like to offer for discussion a refined model [13] of the structure and formation of the Upper Pleistocene-Holocene section, which is based on large volume of seismic profiling data in various part of the Black Sea. Until a comprehensive drilling program exists along a wide range of depths, seismic profiles are the only materials that allow us to link the existing nearsurface sampling and geo-acoustic investigations, deeper seismic exploration studies, and a limited number of drilling in shallow-water regions. Obviously, a seismic stratigraphic model (fig. 1) can have only an approximate character; however, taking into account the constant spatial-geometric basis of such a model, the primary boundaries and their relationships would not change even when future drilling uncovers different lithological and chronological data.
Based on all available data, there are two major events that are ubiquitously recorded in the Upper Pleistocene-Holocene section in various settings, including coastal depressions (straits, bights, limans, incised river valleys) - shelf -alluvial fan - abyssal plain. These events include a large-scale regressive-transgressive cycle of Post-Karangatian-Neoeuxinian age and a regressive-transgressive cycle at the Pleistocene-Holocene boundary. The facts about them are well known as is their global character.
Following is a general evolutionary scheme (fig. 2) for the Black Sea basin during this period (the causes and water balance of regressive-transgressive phases and the special role of Bosporus are not considered in detail because they are the subject of a separate discussion).
The sea level during Post-Karangatian regression was always placed at -(80-90) m by the majority of investigators [22, 23 among others]. Subsequent data on the relict coastal forms of this age found at the edge of the shelf [7, 12 and others] resulted in placing the sea-level position much deeper (maximum: - 155 m). However, it is important to recognize that such a wide range of the discovered coastal landforms correlates with the variable depth of the shelf break itself: from -80 m to -(150-170) m (and even to -200 m). This is mainly the result of expression of multi-directional neotectonic processes and especially
© Glebov A.Yu.1
1 Scientific and Production Association for Marine Geological Operations “Yuzhmorgeologiya”, Gelendzhik, Russia.
t-'ig. 1 Correlation Seismic Stratigrafic Model
Fig. 2. Sea Level Changing
their overprinting by the general process of steady downwarping of the Black Sea depression during Cenozoic and until present along with its expansion [27, 12, 14, 15]. This process is expressed in the subsequent flexure of the continental slope and lowering of the outer shelf up to the formation of the final stage of slump terraces along its edge. Based on this evidence, the model uses an average depth of regression as - 90 m.
During this deep regression, an alluvial fan of the paleo-Kuban River was formed along the NE slope of the Black Sea depression [3]. Its Post-Karangatian development reliably correlates along seismic boundaries from well 379 (DSDP, Leg 42). The calculations of the time and volume of accumulation of the fan and its separate phases lead to the beginning of the last clearly defined sea-level lowstand ca. 14 ky BP. This age brings together the terms “Post-Karan gat” and “Neoeuxinian” and correspond to “Neoeuxinian I” proposed by Fedorov [10]. The duration of this last phase of Neoeuxinian “sea-lake” is estimated to be 3-4 ky [22], which corresponds to eustatic sea-level data (the level of the World Ocean before the transgression was 90-95 m lower than present during 11-12 ky BP [9, 5]); it also corresponds to the conclusion about the initiation of the subsequent transgression ca. 11 ky BP, which was proposed on the basis of highly detailed investigation near the Bosporus region of the Black Sea [1]. The 11 ky BP age is sufficiently well known for its geochronological significance in a number of aspects and is even accepted as the Pleistocene-Holocene boundary [24].
Therefore, approximately 11 ky BP (and possibly earlier, but not prior to 14 ky BP), the eustatic sea-level rise has begun. It left a sufficiently clear footprint in the shelf section as a reflection horizon “2”. Subaerial paleorelief forms and seismic facies are found below this boundary. Above the boundary, the base of the overlying sequence contains nearshore accumulation forms and shallow-water seismic facies of the fluctuating-advancing transgressive sea. Higher in the section, they are replaced by parallel-bedded transgressive seismic facies. The thickness of this entire transgressive seismic-stratigraphic complex of Neoeuxinian deposits on the pre-Caucasus shelf is more than 14 m. During the same time, a layered sequence was formed within the Kuban alluvial fan. According to drilling data on the NW shelf, in the limans of the northern Black Sea plain, in Novorossiysk and Gelendzhik bights the maximum of Neoeuxinian transgression of this cycle reached (10-8) m [29, 19, 16, 12]. The absolute age of ingressive Neoeuxinian deposits in the limans is 8.2 ka [29].
The suggested model accepts as the averaged quantitative evaluation, the period of transgression as from 11 ky BP to 8.2 ky BP, and its amplitude as from - 90 m to - 10 m below the present level. Based on that assessment, an average speed of sea level rise is estimated as about 29 mm per year. Taking into account the minimal decline of the sea bed (0.3° observable on the northwestern part of the Black Sea only) the flooded coastal area could reach 63 m per year. This evaluation does not take into account sea level oscillations detectable in the geological sequences.
Before the Neoeuxinian age came to a close, a regression occurred that was evidently linked with Pereslav cooling (western Europe analog “Piottino
Stage”). The layers of this interval - between Younger Dryas and Boreal “Super-YD horizon”, or “second half of Pre-Boreal” [6]. Although much less substantial than the preceding glaciation, this anomalous event with its cold and dry conditions occurred at 8.2 ky BP. From [18, p. 23]: “The Younger Dryas is followed by a brief return to warm, moister conditions (early Ilolocene), then cooler, drier conditions again (the so-called 8200 yr BP event (Alley et al., 1993; von Grafenstein et al., 1999)”.
Traces of reworking between Neoeuxinian (Pleistocene) and Chernomorian (Holocene) deposits in the nearshore regions have been documented virtually everywhere. In seismic profiles, reflection horizon “1” corresponds to this cycle and is traced to a maximum of - 47 m. It is highlighted by the buried fluvial paleo-channels with depths of incision at - (50-52) m, which were revealed during the latest investigations along the pre-Caucasus shelf. This level corresponds to a previously suggested regression to a depth of - 55 m (“Kolkhida regression” [26, 30]). It is this level (approx.- 50 m) which is often accepted as a pause/deceleration in the Neoeuxinian transgressive phase of the aforementioned earlier cycle. It is interesting to note that in its time and amplitude (-50 m) this regression correlates with Mangyshlak regression in the Caspian Sea.
Below - 50 m on the shelf (it is this region that was studied by the proponents of the “Flood” theory), there are no observed traces of the interruption within the Pleistocene-IIolocene section [22], i.e., marine conditions persisted there. However, this region had shallow-water conditions during the maximum regression. It resulted in the formation of a sharply expressed boundary between Neoeuxinian and Drevnechernomorian [Old Chernomorian] strata [22], appearance of signs of reworking along this boundary within the upper portions of older subaqueous sandbars [8], and extensive input of terrestrial relics into this area noticed by the authors of the “Flood” hypothesis [20, 21]. The maximum water depth along the shelf edge at this time perhaps did not exceed - 30 to -35 m, i.e., the modern depth of wave reworking in the Black Sea (if we consider signs of reworking of the outer ridges on the Bulgarian shelf, mentioned by Dimitrov et al. [8]). The occurrence of all these shallow features at the present depths of about - 100 m is defined by the arithmetics of modern bathymetry (35 m + 50 m = 85 m) with the addition of the aforementioned neotectonic subsidence of the outer shelf. Therefore, the - 100 m depth can hardly be considered the “initial mark” of the subsequent “Flood”. The transgression had occurred, but the infilling of the Black Sea began from the level of approximately - 50 m.
The time of the initiation of this transgression, according to averaged estimates of the absolute age of Neoeuxinian and Drevenechernomorian deposits, can be placed convincingly around 7 ky BP [22]. In this regard, the youngest Neoeuxinian marine facies were deposited transgressively over the surface of reworking (reflection horizon “1”). They reached the - 20 m mark, which is often accepted as a maximum level of the Neoeuxinian transgression, combining two cycles (starting at 14-11 ky BP). Changes in sedimentation regime during the transgression (wave reworking of loosely consolidated sediments along
geologically “recently” exposed shelf; developing changes of the balance toward Mediterranean waters) resulted in accumulation of a 2-m-thick “drape” [20] or "Unit ID” [1]. It began forming from the edge of the shelf of a shallow pre-Holocene sea and caused “excellent preservation” [7] of nearshore features. These forms, when viewed in detail, are more ancient and correspond to the bpginning of the Neoeuxinian transgression of the first cycle. Their expression in the modern relief, as well as in the upper parts of the section, is the result of sediment draping processes.
The transgression reached the point of maximum distribution of Neoeuxinian deposits of the preceding cycle - (10 - 8 m) at the end of Drevnechernomorian (Bugazian-Vityazevian) age according to drilling data, i.e., to ca. 6 ky BP. Therefore, the averaged interval of this regressive-transgressive cycle at the Upper Pleistocene-Holocene boundary, which can be used to calculate the rate of sea-level rise, is from 8.2 to 6.0 ky BP. From the standpoint of the “Flood” theory, it is not clear how a regressive-transgressive cycle with a 100m amplitude would fit into such a short time interval, as well as how to explain the cause and mechanism of not only the transgression but, in this case, also a “catastrophic” regression. It is important to note that neither such substantial amplitudes have been observed in sea-level changes of the World Ocean. In order to calculate the rate of transgression, its beginning is taken as the middle of the above interval, i.e., 7.1 ky BP, although it should be noted that in the Black Sea the regressive phases are shorter than transgressive [25]. The depth interval used for estimating the transgression rate is taken to be - 50 to - 10 m. This allows us to estimate an average rate of sea-level rise on the order of 36 mm/year. For minimal bottom gradients of 0.3c, which exist only on the NW shelf, the rate of land submergence may have reached 78 m/ year.
Despite the fact that our model only estimates the order of ti'ansgression rate, it is possible to discuss whether the annual flooding of 80 m along a more populated NW part of the Black Sea can be considered a “Catastrophic Flood”. Here it is also important to take into account a possibility of seasonal catastrophes linked to wind-driven surges, which can be significant in the shallowest areas. However, it is more likely that with refinement of the timing of transgressive phases in the model they will become longer, thereby decreasing the calculated rates of sea-level rise and consequently the area of submergence.
In conclusion, it is worth mentioning that there exists a colossal amount of factual materials, however there is no “key” database, i.e., a strategic drilling in already noted vital regions, which would put to rest the diversity of theoretical propositions.
1. Aksu A.E., Hiscott R.N., Kaminski M.A., Mudie P.J., Gillespie H., Abrajano T., Yasar D. 2002. Last glacial-Holocene paleoceanography of the Black Sea and Marmara Sea: stable isotopic, foraminiferal and coccolith evidence. Marine Geology N 190.- P. 119-149.
2. Alley R.B., Meese D.A., Shuman C.A., Gow A.J., Taylor K.C., Grootes P.M., White J.W.C., Ram M., Warfdington E.D., Mayewski P.A., Zielinski G.A. 1993. Abrupt
increase in Greenland snow accumulation at the end of the Younger Drvas event. Nature N 362.- P. 527-529.
3. Andreev V.M., Glebuv A.Yu., Shelling S.K. 2000. Paltei'iis of Lute Quaternary glacio-eustatic changes revealed in Kuban deep-water fan seismic records / 1st Plenary Meeting of Project 1GSP 521 (International Geo Science Programme UNESCO-IGSP-IUGC) “Black Sea-Mediterranean corridor during the last 30 ky: sea level change and human adaptation”. (Istanbul - Turkey, October 8-15, 2005).- TUBITAK, Turkey 2006 - P. 6-7.
4. Balabanov I.P., Kvirkvelya B.D., Ostrovskiy A.B. 1981. Resent history of the forming of geological engineering conditions and long-range forecast of the development of coastal zone peninsula Pitsunda. Tbilisi: Mecniereba, 202 p. (In Russian).
5. Bard E., Hamelin B., Fairbanks R.G. and Zindler A. 1990. Calibration of the UC timescale over the past 30,000 years using mass spec-trometric U-Th ages from Barbados corals. Nature N 345, P. 405-410.
6. Chebotareva N.S., Makarycheva I.A. Poslednee oledenenie Evropy i ego geokhronologiia [Last Glaciation of Europe and Its Geochronology] Moscow - Nauka. 1974 (In Russian).
7. Dimitrov P.S. Novi danni za stroezha i vozrastta na niakoi morski akumulativni formi na bulgarskiia Chernomorski shel’fa [New data about the structure and age of marine accumulationform of the Bulgarian Black Sea shelfj. Problemi na Geografiiata 1978.- P.2.- 42-50. (In Bulgarian)
8. Dimitrov P.S., Dimitrov D.P., Solakov D.P., Peichev V.D. Noveishaia geologicheskaia istoriia Chernogo moria i problema potopn [New geological histoty of the Black Sea and problem of flooding]. Geologiia i poleznie iskopaemie mirovogo okeana [Geology and miner resources of the World Ocean]. 2005. N 1 - P. 102-10. (In Russian).
9. Fairbanks, R.G. 1989. A 17,000-year glacio-eustatic sea level record: influence of glacial melting rates on the Younger Dryas event and deep-ocean circulation. Nature N 342(6250) - P. 637- 642.
10. Fedorov P.V. Pozdnechetvertichnaia istoriia Chernogo moria i razvitie iuzhnykh morei Evropy [Late Quaternary history of the Black Sea and southern seas of Europe). In Kaplin P.A., Shcherbakov F.A. (eds). Paleogeografiia i otlozheniia pleistotsena iuzhnykh morei SSSR [Paleogeography and Deposits of the Pleistocene of the Southern Seas of the USSR]. Moscow.- Nauka.- 1977 - P. 25-32. (In Russian).
11. Filipova-Marinova, M., Christova, R., Bozilova, E. Paleoecological conditions and sea level changes in the Bulgarian Black Sea zone during the Quaternary. Proceedings of the Third International Congress “Environmental Micropaleontology, Microbiology and Meiobenthology”. 2002, September 1-6, in Vienna, Austria.- P. 74-77.
12. Glebov A.Yu. Geologicheskoe stroenie shel’fa severo-vostchnoi chasti Chernogo moria (na uchastke mys Opuk-mys Idokopas [Geological Structure of the Northeastern Black Sea Shelf]. Diss. kand. geol.-mineral, nauk, Yuzhmorgeologiia, Gelendzhik. 1987 (In Russian).
13. Glebov A.Yu., Shelting S.K. Sea-level changes and coastline migrations in the Russian sector of the Black Sea: application to the Noah’s Flood Hypothesis. In “The Black Sea Flood Question. Changes in Coastline, Climate and Human Settlement”. Yanko-Hombach, V.; Gilbert, A.S.; Panin, N.; Dolukhanov, P.M. (Eds.). Published by Springer, The Netherlands. 2007.- P 731 775.
14. Glebov A. Yu., Shimkus K.M., Komarov A.V., Chalenko V.A. Istorna i tendentsii razvitiia Prikavkazskoi obiasti Chernogo moria [History and tendency of evolution of Caucasus region of the Black Sea]. In Glumov I.F., Kochetkov M.V. (eds), Tekhnogennoe zagriaznenie i protsessy estestvennogo samoochishcheniia Prikavkazskoi zony Chernogo moria [Man-made Pollution and Process of Natural Self-Cleaning of the Caucasus Zone of the Black Sea]. Moscow. Nedra. 1996.- P. 28-56. (In Russian).
15. Glebov A.Yu., Shimkus K.M., Evsyukov Yu.D. Rel’ef dna i ego formirovanie [The bottom relief and its formation]. In Glumov I.F., Kochetkov M.V. (eds), Tekhnogennoe zagriaznenie i protsessy estestvennogo samoochishcheniia Prikavkazskoi zony Chernogo moria [Man-made Pollution and Process of Natural Self-Cleaning of the Caucasus Zone of the Black Sea].- Nedra, Moscow. 1996.-P. 13-27, (In Russian).
16. Inozemtsev, Yu.I., Ya.K. Lutsiv, E.V. Sobotovich, N.N. Kovalyukh, and L.V. Petrenko. Geochronologiia i fatsialnie kompleksi golotsena Chernomorskoi oblasti [Holocene geochronology and facies complexes of the Pontic area]. In Shnyukov E.F. (ed), Izuchenie geologicheskoi istorii i protsessov sovremennogo osadkoobrazovaniia Chernogo i Baltiiskogo morei [Study of the Geological History and Processes of Recent Sedimentation in the Black and Baltic Seas], Naukova Dumka, Kiev. 1984.- Part 1 - P. 103-113. (In Russian).
17. Lericolais G., Popescu I., Panin N.. Guichard F., and the ASSEMBLAGE Scientific Team. Questions on the sea level fluctuations in the Black Sea since the Last Glacial Maximum Assemblage Project. In Yanko-Hombach V., GurmbS M., Ertuii3 A., McGann M., Martin R., Jacob J., Ishman S. (eds), Fourth International Congress on Environmental Micropalaeontology, Microbiology, and Meiobenthology, Program and Extended Abstracts, 2004. - P. 123.
18. Major C. O., Ryan W. B. F.. Lericolais G., Hajdas I. Constraints on Black Sea outflow to the Sea of Marmara during the last glacial-interglacial transition. Marine Geology, 2002.- N 190(1-2) - P. 19-34.
19. Palatnaya N.N. Vliianie kolebanii urovnia Chernogo moria na formirovanie donnykh osadkov v limanakh severnogo Prichernomor’ia [Influence of Black Sea level changes on the accumulation of bottom sediments in the limans of the northern Black Sea coast]. In Izmeneniia urovnia moria [Sea Level Fluctuations!, P.A. Kaplin, ed., Moscow, Izdatel’stvo Moskovskogo Universiteta, 1982 - P. 279-285. (In Russian).
20. Ryan W. B. F., Pitman W. C. IIIrd, Major C. O., Shimkus K. M.. Moskalenko V., Jones G. A., Dimitrov P. S., Gorbr G., Sakin3 M„ Ybce H. An abrupt drowning of the Black Sea shelf. Marine Geology. 1997., N 138(1-2) P. 119-126.
21. Ryan.W.B.F., Major.C.O., Lericolais,G., & Goldstein.S.L. Catastrophic Flooding of the Black Sea. Annu. Rev. Earth Planet. Sci., 2003., N 31.- P. 525-54.
22. Shcherbakov F.A., Kuprin P.N., Zabelina E.K., Skiba S.I., Parunin O.B. Paleogeografiia Azovo-Chernomor’ia v pozdnem pleistotsene i golocene [Paleogeography of Azov-Black Sea region in Late Pleistocene-Holocene]. In Kaplin P.A., Shcherbakov F.A. (eds), Paleogeografiia i otlozheniia pleistotsena yuzhnikh morei SSSR [Paleogeography and sediments of Pleistocene of the southern seas of the TJSSSR], Moscow., Nauka, 1977.- PP. 51-60.
23. Shcherbakov FA., Kuprin P.N., Potapova L.I., Polyakov A.S.. Zabelina E.K., Sorokin V.AI. Osadkonakoplenie na kontinental’noi okraine Chernogo moria [Sedimentation on the Continental Shelf of the Black Sea]. Nauka, Moscow., 1978. (In Russian)
24. Shimkus K.M. Osadkoobrazovanie Sredizenmogo moria v pozdnechetvertichnoe vremia [Late Quaternary Sedimentation in the Mediterranean Sea]. Nauka, Moscow., 1981. (In Russian).
25. Sobotovich E.V. Radiouglerod v morskikh issledovaniiakh [Radiocarbon in marine investigations], In Starostenko V.I., Geologicheskie problemy Chernogo noria [Geological problems of the Black Sea], Kiev. Academiia Nauk Ukrainy., 2001.- P. 145-164., [In Russian].
26. Tsereteli D.V. Sopostavlenie poslelednikovoi (golotsenovoi) istorii Chernogo I Baltiiskogo morei [Correlation of post glacial (Holocene) history of the Black and Baltic Sea]. Baltica, N 5,. Vilnus , 1974.- P. 205-211.
27. Tugolesov DA., Gorshkov A.S., Meisner L.B., Soloviev V.V., Khakhalev E.M. Tektonika mezozoisko-kainozoiskikh otlozhenii Chernomorskoi vpadini Tectonics Mezozoic-Cenozoic deposits of te Black Sea depression]. Nedra, Moscow., 1985. [In Russian].
28. Von Grafenstein U„ Erlenkeuser H., Brauer A., Jouzel J., Johnsen S.J.. A mid-European decadal isotope-climate record from 15 500 to 5 000 years B.P. Science.. 1999 - N 284.- P. 1654 1657.
29. Voskoboinikov V.M., Rotar' M.F., Konikov E.G. Sviaz’ ritmichnosti stroeniia toishch golotsenovykh otlozhenii Prichernomorskikh limanovs kolebatel’nym rezhimom urovnia Chernogo moria [Relationship between the rhythmic composition of thick Holoccne layers of the Black Sea region lagoons and the oscillatory level regime of the Black Sea]. In Kaplin P.A., Klige R.K., Chepalyga A.L. (eds) Izmeneniia urovnia moria [Changes in Sea Level]. Izdatel’stvo Moskovskogo Gosudarstvennogo Universiteta, Moscow, 1982.- P. 264-274. (In Russian).
30. Yanko V., Troitskuya T.S. Late Quaternary Foraminifera of the Black Sea. Nauka, Moscow., 1987. (In Russian).
Предлагается к обсуждению уточненная сейсмостратиграфическая модель строения и формирования верхнеплейстоцен-голоценовой части разреза Черного моря. Выделяются два крупнейших события, повсеместно запечатленных в разрезе: значительный по масштабу регрессивно-трансгрессивный цикл посткарангат-новоэвк-снпского времени и регрессивно-трансгрессивный цикл на рубеже плейстоцена-голоцена.
Пропонується до обговорення уточнену сейсмостратиграфічну модель будови і формування верхньоплейстоцен-голоценової частини розрізу Чорного моря. Виділено дві найкрупніші події, повсюдно віддзеркалені у розрізі: значний за масштабом регресивно-трансгресивний цикл післякарангат-новоевксинського часу та регресивно-трансгресивний цикл на рубежі плестоцену-голоцену.
