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7
ISSN 2617-2909 (print) ISSN 2617-2119 (online)
Journ.Geol.Geograph.
Geology, 28(2), 241-249.
doi: 10.15421/111925
Kseniia Bondar, Bogdan Ridush, Mania Baryshnikova, Yana Popiuk Journ. Geol. Geograph. Geoecology, 28(2), 241-249.
On palaeomagnetic dating of fluvial deposits in the section of Neporotove gravel quarry on the Middle Dniester
Kseniia Bondar1, Bogdan Ridush2, Mania Baryshnikova1, Yana Popiuk2
1 Taras Shevchenko National University of Kyiv, Kyiv, Ukraine
2 Yuriy Fed'kovych Chernivtsi National University, Chernivtsi, Ukraine e-mail: [email protected], [email protected]
Received: 12.04.2019 Abstract. The paper presents the results of palaeomagnetic studies of Quaternary non-
Received in revised form: 03.05.2019 cemented deposits from the section of Neporotove on the VIIIth terrace of the Dniester Accepted: 12.05.2019 River valley with abnormal thickness (more than 20 m) of the channel alluvium near the
village of Neporotove, located on the right bank of the Dniester River. Alluvial facies of river terraces' deposits are valuable palaeogeographic archives but not quite complete. They are affected by denudation and often do not contain fossils. The possible way for their dating is provided by a palaeomagnetic method performed on suitable for sampling underlying and overlying beds. The alluvial sequence consists of four units. Unit I is composed of inclined gravel-pebble layers with the sand filler with a visible thickness of about 8 m. Unit II has bedded over the denudated surface of Unit I; it consists of light-yellow laminated aleurit loam, 5-30 cm thick underlaid by 0.5-1.5 bed of fine sand. We consider Unit II to be lacustrine deposits accumulated in quiet water. Unit III is represented with inclined or sub-horizontally layered gravel-pebble-boulder deposits with up to 10 m of visible thickness. It includes boulders and blocks of sedimentary rocks up to 1.0 in diameter, considered as drop-stones. In the roof of the gravel-pebble Unit III, there is the white carbonate layer, probably, the illuvial horizon of the palaeosol (mr1), which transited up into the brownish-red horizon A (Unit IV). Unit IV - dark-red sandy-gravel horizon, pedosediment, probably partly the reworked material washed into ice wages in the roof of Unit III. As a result of alternating field stepwise demagnetisation of natural remanence of sediments, we determined that loamy Unit II, which separates members of gravel stratum, and sandy Unit IV, which overlays packs of gravel alluvium, bear characteristic remanent magnetisation (RM) with normal geomagnetic polarity. Taking into consideration lithology and two-fold structure of terrace gravel alluvium as well as palaeomagnetic results, we assume the lacustrine deposits of Unit II was formed during Jaramillo palaeomagnetic subchron corresponding to the end of Shyrokyne Stage, and a pedosediment of Unit IV was formed during Martonosha Stage. The upper alluvial suite of a terrace (Unit III) was generally deposited during a cold stage, directly prior to the onset of lacustrine loam sedimentation, while the lower alluvial member (Unit I) dates from the preceding warm stage. Thus, we defined the geological age of the whole channel alluvium strata of the VIIIth Dniester terrace as Shyrokyne-Pryazovya Stage.
Keywords: Dniester River, Neporotove gravel quarry, river terrace, palaeomagnetic dating, channel alluvium, remanent magnetisation
Про палеомагнггне датування (флнншальипх вiдкладiв у po3pi3i гравшного кар'еру Непо-ротове на Середньому Дшстр^
Ксешя Бондар1, Богдан Рщуш2, М^я Баришшкова1, Яна Поп'юк2
1 Кигвсъкий нацюналъний ушверситет iMeHi Тараса Шевченка, Кигв, Украта
2 Чершвецъкий нацюналъний ушверситет iмeнi Юрiя Федъковича, Чершвщ, Украта e-mail: [email protected], [email protected]
Анотащя. У po6oTi представлеш результаты палеомагштних дослщжень четвертинних пухких вiдкладiв з p03pi3y VIII-i надзаплавно'1 тераси долини Дшстра з надпотужними (понад 20 м) шарами руслового алювш бшя села Непоротове, що на правому беpезi Днютра. Алювiальнi фаци вiдкладiв piчкoвих терас е щнними палеoгеoгpафiчними аpхiвами, але часто не повними. Значна частина вiдкладiв зникае внаслщок денудаци, флювiальнi шари переважно е палеонтолопчно шмими. 1хне датування можливе за допомогою палеомагштного методу, коли вш застосовуеться на придатних для вщбору зразюв шдстеляючих та перекриваючих вщкладах. Рoзpiз алювiальних вiдкладiв у Непоротовому складаеться з чотирьох верств. Вер-
Ä ^^eology.
Journal of Geology Geography and Geoecology
Journal home page: geology-dnu-dp.ua
ства I являе собою косошарувату гравшно-галечникову товщу з пщаними прошарками та видимою потужтстю близько 8 м. Верства II залягае на денудованш поверхн верстви I, вона складаеться з свггло-жовтого горизонтально шаруватого суглинку товщиною 5-30 см, який тдстелюеться 0,5-1,5 м шаром др1бного шаруватого тску. Верства II складена озерними в1дкладами, накопиченими в спокшних водних умовах. Верства III представлена похилими або субгоризонтально-шаруватими гравшно-галечно-валунними вщкладами з видимою товщиною до 10 м. Вона мгстить валуни i брили осадових порщ д1аметром до 1.0 м, яю ми вважаемо дроп-стоунами. У TO^iKn галечника верстви III знаходиться бший карбонатний прошарок - ймовiрно, шкшальний горизонт мартоноського викопного Грунту (mrД який догори переходить у бурувато-червоний горизонт А (верства IV). Верства IV -темно-червоний пщано-гравшний горизонт, педоседимент. Складаеться з переробленого матерiалу, вмитого до морозобшних трiщин в покрiвлi верстви III. У результата магштно! чистки зразюв пухких вiдкладiв змiнним полем встановлено, що i суглиниста верства II, яка роздшяе пачки гравшно! товщi, i пщана верства IV, яка перекривають пачки гравшного алювта, мають пряму характеристичну намагтчешсть. Враховуючи подвшну будову руслового алювта, а та-кож палеомагнiтнi результати, було висунуто припущення про приналежтсть шару II озерних вiдкладiв до субхрону прямо! полярност Харамшьо, який стратиграфiчно вiдповiдае верхньому широкинському тдетапу, а педоседименту IV до мартоноського палеоктматичного етапу. Верхнiй терасовий алювш (верства III) накопичився тд час холодно! стади, безпосередньо перед початком освдання озерного суглинку, тодi як нижнш алювiй (верства I) датуеться попереднiм теплим етапом. Отже, геолопчний вiк всiе! товщi руслового алювта VIII-! тераси визначено як широкинсько-приазовський.
Ключовi слова: pium Дтстер, гравтний кар'ер Непоротове, piuKoea тераса, палеомагнтне датування, русловий алювш, за-лишкове намагтчення.
Introduction. Alluvial facies of river terraces' deposits are valuable palaeogeographic archives containing records about the history of the formation of these rivers' valleys and climate change during corresponding periods. The lithofacial composition, stratigraphy, structure of the alluvium reflects the interaction of many processes, such as short-term migrations of individual channels to long-term vertical tectonic movements (Matoshko et al., 2004; Mial, 2006). Meanwhile, like most other types of continental deposits, the alluvial archives are not quite complete, as they are affected by denudation. In particular, they often do not contain fossils, being palaeontologically mute. The palaeomagnetic method performed on suitable for sampling underlying and overlying beds provides a possible way for their dating.
We examined a terrace section near the village of Neporotove, where previously the abnormal thickness of the channel alluvium exceeding 20 m was described (Ridush, Popiuk, 2015). As described in the literature, the channel alluvium strata in the terrace sediments of the middle part of the Dniester valley usually does not exceed several meters, and only occasionally, together with the floodplain facies, reach up to 15-16 m (Veklych, 1982). Just in the lower reaches of the Dniester the so-called "Tiraspol gravel" is known -the river channel alluvium facia of Kolkotovo terrace, which is up to 15 m thick (Nikiforova et al., 1971). So, we faced the question of elucidating the age and the genesis of these strata, and their position within existing schemes of floodplain terraces.
This study reports the examination of characteristic magnetic remanence values in two layers of fine non-cemented sediments separating and overlaying coarse channel alluvium strata to
estimate their magnetostratigraphic position relative to Brunhes-Matuyama geomagnetic polarity reversal. It leads to the dating of the Vlllth Dniester terrace. Materials and methods. Many researchers studied the terraces of the middle reaches of the Dniester valley. The history of these studies is described in detail by O. Tomeniuk (2010). Her publication contains a comparison of the numbers and heights of terraces by different authors. So, within the middle part of the Dniester River valley Yu. Polyansky (1929) and S. Rudnytsky determined six terraces, R. Vyrzhykivskyi (1933) and I. Hofstein (Hofstein, 1979) - seven terraces, I. Ivanova (1969) - eight terraces, A. Yatsyshyn and A. Bogutsky (2008) - seven terraces, P. Gozhik and L. Lindner (2007) - thirteen terraces, M. Veklych (1982) - sixteen terraces. In this paper, we use the scheme of terraces by M. Veklych (1982), which, moreover, is used in State Geological Surveys in Ukraine.
Neporotove section. Previously the section was described by B. Ridush and Y. Popiuk (2015). The gravel outcrop uncovered by a quarry located on the northern outskirts of the Neporotove village (Sokyryany district, Chernivtsi region, Ukraine) (Fig. 1). Coordinates ofthe outcrop are N 48°36'32.47", E 27°17'11.22". Bedrocks represented with: Proterozoic shales with the inclusions of phosphorite nodules; Cretaceous deposits of varying lithological composition, among which is gaize with inclusions of flint nodules; Sarmatian detrital and tortoiseshell limestones.
Although the Quaternary gravel-pebble stratum is generally fairly homogeneous, it is nevertheless divided into two horizons by light-yellow, finegrained laminated aleuritic loam (Unit II, Fig. 2, II),
The alluvial sequence consists of four units.
Fig. 1. Location of the Neporotove section of terrace deposits.
Unit I beds on the denudated surface of Ediacaran shale. It is composed of an inclined (the angle of approximately 30°) gravel-pebble layers with a sand filler (up to 20-30% of the volume), with a visible thickness of about 8 m. Gravel and pebble stones are generally well-rounded and sub-rounded. The layers usually are 10-20 cm thick, with larger and smaller sand content, between which there are no clear boundaries, alternate down the section.
Unit II has bedded over the denudated surface of Unit I. It consists of light-yellow laminated aleurit loam, 5-30 cm thick, which is here and there underlaid by lenses (up to 0.5-1.5 m thick) of finegrained yellow and grey sand with gravel and pebble inclusions. We assume the lacustrine genesis of this stratum. It is evident that the loamy layer is quite dense and water-resistant, since directly over it in the covering gravel Unit III some suffosion channels with a diameter of 0.4-0.7 m have been traced.
Unit III - inclined (angle about 20°) or sub-horizontally layered gravel-pebble-boulder deposits, with or without sand filler (up to 10%), with up to 10 m of visible thickness. It lays with disconformity on the surface of Unit II, and, where Unit II is absent, on the surface of Unit I. There are overlapping layers of
different granulometric composition: coarse pebbles, fine pebbles, gravel. Numerous inclusions (up to 10%) of weakly rolled and non-rolled boulders of Sarmatian and Cretaceous limestones and sandstones, sometimes Devonian sandstones or quartz, with a diameter of 0.81.0 m or more. There are pellets of Proterozoic dark grey, dark green, light green argillites in size from large pebbles to small boulders up to 0.5 m in diameter included in the strata. Among the pebble material, the weakly-rolled flint pebbles with traces of cryogenic weathering predominate (no less than 50%). Lithology of gravel and pebble material is also represented by Devonian red sandstones, Sarmatian limestones, light Cretaceous limestones and sandstones. Presence of argillite pellets indicates that the flood (or floods) was extreme and the water jet tore out the fragments of argillite rocks, rather than picking up the products of weathering of argillite, which would take place under a usual flood. The large boulders we consider as dropstones, transported by river-ice. In the roof of Unit III, the ice wedges up to 1 m deep are often. In the roof of the gravel-pebble Unit III, there is the white carbonate layer, probably, the illuvial horizon of the palaeosol (mr1), which transited up into the brownish-red horizon A (Unit IV).
Fig. 2. Gravel-pebble alluvium at the Neporotove outcrop. I - Unit I, the lower gravel-pebble bed of low-angle cross-bedding; II - Unit II, the loam layer, light yellow, laminated; III - Unit III, the upper gravel-pebble bed of low-angle cross-bedding, with domination of macro-fragmental material and drop-stones at the roof of the bed; IV - dark-red sandy-gravel, V - Unit V subaerial loess deposits of unknown age (Ridush, Popiuk, 2015). The scale stick on the photo is 2 m long.
Unit IV - dark-red sandy-gravel horizon, probably partly the reworked material of Unit III, coloured by the illuvium of red palaeosol, here and there washed into ice wages in the roof of Unit III. Thickness is around 0.4-0.6 m.
From 1.0 to 4.0 m of loess and loess loams of undefined age are deposited above (Unit V).
Sampling and measurements. Since the gravel-pebble deposits of Units 1 and 3 are not suitable for
paleomagnetic examination, we focused on sampling Units 2 and 4 in order to achieve the objectives of the study. From the horizontally-layered loamy Unit II, we cut two samples from two stratigraphic levels, from which in the laboratory we drilled six 2.5 cm specimens for palaeomagnetic measurements using the standard procedure (Butler, 1992).
From the reddish sandy Unit IV at the top of the upper gravel-pebble layer we manually cut nine
Fig. 3. Examples of AF-demagnetization of specimens from Unit II: (A) characteristic Zijderveld plot and NRM decay curves during AF demagnetization (B).
2.5 cm cylinder specimens. A magnetic compass was used to provide an unequivocal in situ geographic orientation of each manually cut sample.
The measurements were performed in the Ivar Gi^ver Geomagnetic Laboratory at the University of Oslo (Oslo, Norway) and the magnetic laboratory of ESI «Institute of Geology» of the Taras Shevchenko National University of Kyiv (Kyiv, Ukraine).
The magnetic susceptibility (k) of all samples was measured on Geofyzika KLY-2 Kappabridge.
The remanent magnetisation of specimens was measured using a three-axis WSGI Model 755 SRM (WSGI, USA) cryogenic rock magnetometer. The stable characteristic remanent magnetisation (ChRM) of samples was isolated by stepwise alternating field demagnetisation in a 2G demagnetizer (with steps of 2.5-10 mT until 70 mT for specimens from Unit II and 100 mT for specimens from Unit IV).
The Keonigsberger ratio (Q=NRM/Ji, Ji -induced magnetization) characterising relative magnetic hardness of the material (Evans and Heller, 2003) was calculated.
Results. Since the fluvial sediments represent the re-deposited in shallow water loamy and sandy material, their characteristic remanent magnetisation is rather depositional (DRM) with possible post-depositional (PDRM) contribution. DRM is formed due to the orientation of magnetic particles along the magnetic field during settling in the water and staying in the upper bottom layer until the sediment is compacted. In this case, the vectorial components of the magnetisation - inclination (I) and declination (D) may be biased due to the direction of the waterflow and because of the settling of the elongated magnetic grains when falling on the horizontal bottom. The latter leads to a shallowed I compared
with the geomagnetic field inclination of the time and place of sediment's formation (Tauxe, 2018). The magnetisation of sediments could be formed after the formation of a layer (PDRM). Under certain conditions "rejuvenation" of magnetisation relative to the age of the formation of the loose stratum itself is evidenced by the absence of inclination shallowing (Kodama, 2012).
NRM of loam from Unit II makes 6.2...6.5*10-3 Am, k makes 245...280*10-6 SI un. These values are typical for loess deposits from loess-palaeosol sequences of Ukraine. The NRM is relatively "hard"; the median destructive field (MDF) is 45-55 mT, the Keonigsberger ratio Q is 0.45 ... 0.50. The demagnetization path on the Zijederveld plots exibit almost straight line and is directed toward the origin. The magnetic declination D of the characteristic component (isolated under the AF-demagnetizing procedure in the range of 10-63 mT) is -12...3°; the inclination is shallowed relatively to the inclination of the recent geomagnetic field and makes 38...51°. Examples of Zijderveld plots and NRM demagnetisation curves are shown in Fig. 3.
Thus, we can conclude that the entire stratum bear ChRM with normal geomagnetic polarity, ChRM is probably depositional.
NRM and k of samples from Unit IV demonstrate low values. NRM makes 1,2...4,3*10-3 A/m, k makes 142...242*10-6 SI un. MDF makes 11-14 mT, the Q is 0.16...0.59 indicating presence of low-coercive magnetic mineral. As recognized from NRM decay curves, the remanence of samples probably consists of two components, relatively soft one is presumably viscous, it makes up to 65% of remanence. The demagnetization path on the Zijedrvild plots exibit almost straight line and is directed toward the origin, as both components of the NRM are directed equally.
Fig. 4. Examples of AF-demagnetization of specimens from Unit IV: characteristic Zijderveld plots (A, B) and NRM decay curves during AF demagnetization (C).
The magnetic declination of the harder characteristic component (isolated under AF-demagnetizing procedure in the range of 20-100 mT) is -2...6°, the inclination corresponds to the inclination of the recent geomagnetic field and makes 65...71°. Examples of Zijderveld plots and NRM demagnetisation curves are shown in Fig. 4. We can conclude that the sediment acquired the magnetisation in the period of normal geomagnetic polarity, characteristic RM is probably post-depositional.
Discussion. When considering the possible age of the alluvium, it is crucial to determine which lithological horizon may bear the Matuyama-Bruhnes boundary (MBB) - the main Quaternary benchmark.
It is important to consider modern ideas about the position of MBB, as this will significantly contribute to the correct interpretation of the palaeomagnetic results on the background of climate-stratigraphic evidence from the fluvial facies.
According to the magnetostratigraphic scale of Pleistocene of Ukraine (Tretyak and Vigilyanskaya, 1994), composed on the base of the regional stratigraphic scheme of the loess-palaeosol sequence of the Central Ukraine (Veklych, 1984) the MBB lays in the bottom of Shyrokyne unit. Early palaeomagnetic studies in the area of Lower Dniester put MBB into the loess mantle above the alluvium of the Vlllth terrace (Pevzner and Chepalyga, 1970; Pospelova
Fig. 5. Lithology (A): I - inclined gravel-pebble layers with a sand filler, thickness of about 8 m, II - light-yellow laminated aleurit loam, 5-30 cm thick, III - gravel-pebble-boulder deposits, up to 10 m of visible thickness, IV - dark-red sandy-gravel horizon, thickness around 0.4-0.6; stratigraphy with oxygen isotope stages (MIS) after (Gerasimenko, 2010) (B); magnetic polarity after (Cande, 1995) (C); and climate (D) of Dniester channel alluvium in Neporotove section.
and Gnibidenko, 1972; Trubikhin and Chepalyga, 1986). In the summarising publication (Lindner et al., 2006), which include data on the Upper, Middle, and Lower Dniester reaches, the MBB was lifted to the boundary of the Pryazovya and Martonosha units of Stratigraphic scheme of the Pleistocene of Ukraine (Veklych, 1984).
According to recent studies performed on precise magnetic equipment, the MBB was not distinguished in the section of Prymors'ke (Nawrocki et al., 1999), which is underlain with the soils of the Martonosha unit. The MBB was defined in the upper part of the Martonosha unit in the Dolynske section (Bakhmutov et al., 2005), in the lower part of the Shyrokyne palaeosol in the section of Viazivok (Glavatsky et al., 2016, Bakhmutov, Glavatsky, 2016). However, in the Viazivok section, the Martonosha unit was missed during sampling, and the authors themselves suspect that the palaeomagnetic record could be aged due to
lock-in depth effect. In the section of Roksolany, the MBB was defined at the junction of buried soils of the Lubny and Martonosha units (Bakhmutov, and Glavatsky, 2014; Bakhmutov et al., 2017), relying on the temperature demagnetisation of RM. But authors also provide the data of AF-demagnetization of RM, according to which the MBB should be determined lower, in the Pryazovya unit. The AF-demagnetization method seems to be preferable for soils and loess since during the high-temperature heating experiment the formation of new minerals occur (Evans, 2003).
Thus, the most reasonable for today is the position of the MBB on the contact between the Pryazovya loess and the Martonosha palaeosol, as presented in the paper (Lindner et al., 2006).
Veklych and Dubniak (1975) considered that on the most of river terraces alluvium has a twofold structure. The uppermost alluvial layer passes upwards into loess with a subaerial palaeosol
developed in its upper part and further burial by a sequence of younger loesses and soils. The upper alluvial suite of a terrace was generally formed during a cold stage, directly prior to the onset of aeolian loess sedimentation, while the lower alluvial member dates from the preceding warm stage. Thus, the alluvium of a terrace corresponds to a certain loess-soil couplet on interfluve areas, i.e. to a particular climatic cycle. Matoshko with co-authors (Matoshko et al., 2004) consider this approach problematic because the evidence from the fluvial facies themselves is neglected in favour of simplistic climate-stratigraphy. Nevertheless, we still use this approach.
The palaeomagnetic record of sediments may provide chronostratigraphic information as sediments may acquire magnetic remanence upon deposition and shortly after deposition.
According to this, the normal polarity sandy Unit IV should be attributed to the Martonosha unit (mr). Without contradicting the geological data, it can be assumed that the normal polarity of Unit II may indicate its formation during the Jaramillo subchron inside the Matuyama Chron of reversed polarity, i.e. in the range of0.99-1.07 million yrs. (Cande and Kent, 1995), which corresponds to the end of the Shyrokyne stage (sh3) (Lindner et al., 2006).
Such an interpretation makes it possible to limit the upper dating of the lower alluvium Unit I to 1.07 million years. So, the Unit I itself can be attributed to the Shyrokyne 1-2 subunits (MIS 24). Going further in our assumptions, let us point out that the erosion of loamy sediments of Unit II and the accumulation of the upper gravel pack of Unit III occurred in Pryazovya Stage (Fig.5).
Conclusion. The layers of non-cemented deposits that separate and overlay alluvium packs were formed during periods of normal geomagnetic polarity. We assume the Unit II of lacustrine deposits we attributed to Shyrokyne-3 unit, the normal polarity zone found here is correlated to the Jaramillo subchron. Unit IV belongs to the Martonosha unit; however, this pedosediment was formed during one of cold Martonosha substages by inwashing the material to frost-cracks in gravel Unit III.
We defined the geological age of the channel alluvium of the VIIIth terrace of the Dniester River as Shyrokyne-Pryazovya.
Acknowledgements. We are grateful to the Ivar Gi^ver Geomagnetic Laboratory (IGGL) for the use of their facilities. The IGGL is funded by the Research Council of Norway (project #226214) and the Centre for Earth Evolution and Dynamics, University of Oslo.
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