Milutin Milankovitch Anniversary Symposium Field Guide Book

…Just as thunderbolt during a dark night illuminates the whole horizon in front of man, so does lighting in the genius open new ideas and new field of science.

Milutin Milankovitch

Milutin Milankovitch was a traveler Through Distant Worlds and Times*. The imagination of the cosmic walker explained basic mechanism of paleoclimatic variations during the Ice age.

Most of his life was linked to the loess area of middle Danube river basin from Vienna town of his education and engineer career to Belgrade place of his most effective scientific work. However, Milutin Milankovitch didn’t know that steep Danube’s loess bank from his born village Dalj to Belgrade preserved one of the most detailed signature of his paleoclimatic cycles on European land during the last about 850 ka.

*Title of Milankovitch’s popular book published in Serbian (Kroz vasionu i vekove) and in German (Durch ferne Welten und Zieten, Briefe eines Welallbummlers).

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Map 1 The Geographical map of area with excursion points

Legend: 1 Loess plateau; 2 Fruška gora Mountain; 3 Main loess exposures; 4 Excursion route

Figure 1 Loess-paleosol exposure of Ruma brickyard

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HOST TOWN

BELGRADE

http://www.beograd.org.yu/english/grad/cinjenice/index.htm

"The sky above Belgrade is wide and high, unstable but always beautiful; even during winter serenities with their icy splendour; even during summer storms when the whole of it turns into a single gloomy cloud which, driven by the mad wind, carries the rain mixed with the dust of panonian plain; even in spring when it seems that it also blooms, along with the ground; even in autumn when it grows heavy with the autumn stars in swarms. Always beautiful and rich, as a compensation to this strange town for everything that isn't there, and a consolation because of everything that shouldn't be there. But the greatest splendour of that sky above Belgrade, that are the sunsets. In autumn and in summer, they are broad and bright like desert mirages, and in winter they are smothered by murky clouds and dark red hazes. And in every time of year frequently come the days when the flame of that sun setting in the plain, between the rivers beneath Belgrade, gets reflected way up in the high celestial dome, and it breaks there and pours down over the scattered town. Then, for a moment, the reddish tint of the sun paints even the remotest corners of Belgrade and reflects into the windows, even of those houses it otherwise poorly illuminates." Written about Belgrade by: Ivo Andrić, Serbian Nobel prize laureate.

Belgrade is situated at the place where the Sava joins the Danube. Belgrade is one of the oldest cities in Europe and, beside Athens and Bucharest, the greatest urban whole of the Balkan Peninsula. Belgrade, a city of very tumultuous history, is one of the oldest cities in Europe. Its history lasts full 7,000 years. The area around two great rivers, the Sava and the Danube has been inhabited as early as palaeolithic period. Remains of human bones and skulls of Neanderthals, found in the stone-pit near Leštane, in a cave in Čukarica and near the Bajloni market, date back to the early Stone Age. Remains of the late Stone Age culture have been found in Vinča, Žarkovo and in Upper Town, above the Sava and Dunav confluence. It indicates that the area of Belgrade has been continually inhabited and that the intensity of the settling has been getting higher and higher. Many of today's settlements in Belgrade surroundings lie on cultural layers of earlier prehistoric settlements. Vinča near Belgrade comes among the most important settlements and cultural sites of the prehistoric period. The presence of Illyrians is characteristic for the Bronze Age. The archaeological excavations at Rospi Ćuprija, Upper Town, Karaburma, Zemun and Vinča confirm hypotheses that the Belgrade area has been intensively inhabited and that its population has been engaged in plough agriculture and other supporting economic activities. Necropolises of the Bronze and Metal Ages as well as the evidence of different cultural influences have been discovered at these locations.

The members of a Celtic tribe founded Singidunum in the III century B.C., while the first record of the name Belgrade dates back to 989 A.D. During its long and tumultuous history, Belgrade has been conquered by 40 armies, and 38 times it has been raised up from the ashes.

Belgrade is the capital of Serbia, having around 1.6 million residents. In the field of traffic and transport, it is a city of the highest importance as a road and railway center, as a port for river and air traffic, and as a telecommunication center. It spreads over 3.6% of the territory of Serbia, and 15.8% of Serbian population lives in this city. Also, 31.2% of all employed workers in Serbia work in Belgrade. Important economic and agricultural capacities are developed in Belgrade, especially metallurgy, metal-working industry and electronic industry,

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then commerce and banking. The free trade zone is located in the wider area of Belgrade, Smederevo and Pančevo, on the banks of the Danube river, covering 2,000 sqm of business space. Also, 30% of the national product of Serbia is made in Belgrade.

Belgrade is the capital of Serbian culture, education and science. It has the greatest concentration of institutions of national importance in the field of science and art. There is the Serbian Academy of Sciences and Arts, established in 1886 as the Serbian Royal Academy: the National Library of Serbia, established in 1832; the National Museum, established in 1841 and the National Theatre, established in 1869. The city is also the seat of the Belgrade University, founded in 1808 as the Great School, and the seat of the University of Art. Belgrade has the status of a separate teritorial unit in Serbia, having its own autonomous city government. Its territory is divided into 16 municipalities, having their own local governmental bodies. The City of Belgrade is the founder, financer and organizer of many regular annual cultural events. Most of the authors from all fields of culture and art live and work in Belgrade, the center of culture and art of Serbia and Yugoslavia. Belgrade has also hosted the famous world authors and performers in the fields of music, theatre, film... The most important works of architecture, monuments and other immovable cultural properties of the Serbian people are in most part located in Belgrade. It is also the seat of the highest state and national institutions of culture and art: Serbian Academy of Sciences and Arts, National Library of Serbia, National Museum, National Theatre and the University of Arts. According to 1991 census, there are 87% Belgrade citizens of Orthodox persuasion, about 2% of Islamic and 2% of Roman Catholic belief, 0.2% of them are Protestants, 0.03% Jews, 6% of unknown belief, while 3% declared as nonbelievers. The most important Orthodox church of Belgrade - the Cathedral Church was built in 1840. Some of the oldest are also the Nikolajevska Church (1745) and the Church of the Holy Mother of God (1783) in Zemun. The monumental St. Sava's Temple, the greatest Orthodox temple, can receive 12,000 believers. By their importance and look, one can also set apart the churches Ružica and Sveta Petka, crkva Svetog Marka, Vaznesenska (Ascension) church, Topčider church and the church of Alexander Nevsky. In the wider city area there are also two old log-cabin churches in the villages of Vranić and Orašac. In the Belgrade area and its wider surroundings, there are several monasteries built at the end of the XV century or later, demolished and rebuilt several times, and mostly wholly or partially, renewed in the last two decades. The monasteries of Rakovica, Presentation of the Most Holy Mother of God, Fenek, Rajinovac and Tresije are beautiful monuments of Serbian past. The monasteries in Slanci, Mislođin and Pavlovac on the slopes of the Kosmaj have been partly renewed. The ruins of the Kastaljan monastery are hardly accessible because the road that leads to them is bad. There are also several Roman Catholic churches, one synagogue, one mosque and several places of worship of other confessions in Belgrade.

The educational system is within the competence of the Republic of Serbia - Ministry of Education and Sport, while a minor part of activities is within the competence of the Secretariat for Education. Belgrade, as a university center, has 2 state universities, and the private institutions for high education are being established, too. There are 278 elementary and secondary schools in Belgrade. There are 196 elementary schools - 162 regular, 15 special, 15 art schools and 4 schools for elementary education of adults. There are also 82 secondary schools - 50 vocational, 19 gymnasia, 8 art schools, and 5 special secondary schools. The educational system covers 230,000 pupils, and 22,000 employees in over 500 school buildings, covering about 1,100,000 sqm. Belgrade is the seat of the highest Serbian scientific and research institutions in all fields.

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STOP 1

THE PALEOCLIMATIC RECORD OF STARI SLANKAMEN LOESS-PALEOSOL SEQUENCE DURING THE LAST 850 ka

Marković B. Slobodan ^{1, Heller Friedrich 2, Kukla J. George 3, Gaudenyi Tivadar 1 &}

Јovanović Мladjen1

1Quaternary research centre, University of Novi Sad, Trg D. Obradovića 3, 21000 Novi Sad, Serbia and Montenegro

2 Institut für Geophysik, ETH Hönggerberg, CH-8093, Zürich, Switzerland

3 Lamont-Doherty Earth Observatory of Columbia University, Rt. 9W, Palisades NY 10964, USA.

1. INTRODUCTION

The pionir paleomagnetic investigations of Central Europe loess (Bucha et al., 1969) have provided cronostratigraphic framework for Kukla’s (1970, 1975, 1977) correlation between paleoclimatic fluctuations recorded in land and deep-see sediments. This was an overture for Chinese loess research "revolution" which started after Heller and Liu (1982, 1984, 1986) published the first reliable magnetostratigraphic zonation of about 2.5 Ma old Luochuan loess column and established magnetic susceptibility (MS) as one of the most sensitive paleoclimatic proxies. Afterward those many paleomagnetic studies of Chinese, Central Asian, European, New Zeland’s, North and South American loess deposits made an advance in reconstruction of Pleistocene natural processes (Heller & Evans, 1995; Evans & Heller, 2001). This research trend detoured around Stari Slankamen loess exposure, in spite of its noticed scientific importance (Bronger, 1976, 2003; Singhvi et al., 1989). Paleomagnetic data presented in this study confirm and moreover emphasize significance of this section for understanding middle and late Pleistocene paleoclimatic history in Central and South-eastern Europe.

Figure 1 Geographical position of Stari Slankamen exposure

Јovanović Мladjen1

1Quaternary research centre, University of Novi Sad, Trg D. Obradovića 3, 21000 Novi Sad, Serbia and Montenegro

2 Institut für Geophysik, ETH Hönggerberg, CH-8093, Zürich, Switzerland

3 Lamont-Doherty Earth Observatory of Columbia University, Rt. 9W, Palisades NY 10964, USA.

1. INTRODUCTION

The pionir paleomagnetic investigations of Central Europe loess (Bucha et al., 1969) have provided cronostratigraphic framework for Kukla’s (1970, 1975, 1977) correlation between paleoclimatic fluctuations recorded in land and deep-see sediments. This was an overture for Chinese loess research "revolution" which started after Heller and Liu (1982, 1984, 1986) published the first reliable magnetostratigraphic zonation of about 2.5 Ma old Luochuan loess column and established magnetic susceptibility (MS) as one of the most sensitive paleoclimatic proxies. Afterward those many paleomagnetic studies of Chinese, Central Asian, European, New Zeland’s, North and South American loess deposits made an advance in reconstruction of Pleistocene natural processes (Heller & Evans, 1995; Evans & Heller, 2001). This research trend detoured around Stari Slankamen loess exposure, in spite of its noticed scientific importance (Bronger, 1976, 2003; Singhvi et al., 1989). Paleomagnetic data presented in this study confirm and moreover emphasize significance of this section for understanding middle and late Pleistocene paleoclimatic history in Central and South-eastern Europe.

Figure 1 Geographical position of Stari Slankamen exposure

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2. LOCALITY DESCRIPTION

The Stari Slankamen section is located in the north-eastern part of Srem loess plateau on the right bank of the Danube river, opposite Tisa (Tisza) junction. Geographical coordinates of the Stari Slankamen site are 45^{o7’58’’ N Latitude and 20o18’44’’ E Longitude (fig. 1).}

Detailed exposure description was presented by Marković-Marjanović (1972), Butrym (1974), Bronger (1976), Butrym et al. (1991) and Marković et al. (in preparation) figure 2. The nearly 40 m thick step loess cliff intercalated with 10 fossil soils. Bronger’s (1976) paleopedological data suggest gradual environmental transition from humide and warm to colder and drier paleoclimate along the Stari Slankamen loess-paleosol sequence deposition. Erosion layer with many small rock blocks is interposed at 1,5 m below of paleosol SL S1 (fig. 2). The same erosion level is visible also at 1.1 km distant exposure in deep loess valley, between Stari and Novi Slankamen. After a careful cleaning of the section during the field investigation in 2004, we observed that erosion event caused missing of lower part of loess horizon SL L2, paleosol SL S2 and upper part of loess unit SL L3.

Figure 2 Comparison of Stari Slankamen loess-paleosol sequence descriptions 1. Marković-Marjanović (1972); 2. Butrym (1974); 3. lithology according to Bronger (1976) TL ages after Singhvi et al. (1989); 4. Butrym et al. (1991); 5. our interpretation

Marković and Kukla (1999) designed the units according to names which follow the Chinees loess stratigraphic system (Kukla, 1987) but carry the prefix "SL", referring to the Stari Slankamen site.

Detailed exposure description was presented by Marković-Marjanović (1972), Butrym (1974), Bronger (1976), Butrym et al. (1991) and Marković et al. (in preparation) figure 2. The nearly 40 m thick step loess cliff intercalated with 10 fossil soils. Bronger’s (1976) paleopedological data suggest gradual environmental transition from humide and warm to colder and drier paleoclimate along the Stari Slankamen loess-paleosol sequence deposition. Erosion layer with many small rock blocks is interposed at 1,5 m below of paleosol SL S1 (fig. 2). The same erosion level is visible also at 1.1 km distant exposure in deep loess valley, between Stari and Novi Slankamen. After a careful cleaning of the section during the field investigation in 2004, we observed that erosion event caused missing of lower part of loess horizon SL L2, paleosol SL S2 and upper part of loess unit SL L3.

Figure 2 Comparison of Stari Slankamen loess-paleosol sequence descriptions 1. Marković-Marjanović (1972); 2. Butrym (1974); 3. lithology according to Bronger (1976) TL ages after Singhvi et al. (1989); 4. Butrym et al. (1991); 5. our interpretation

Marković and Kukla (1999) designed the units according to names which follow the Chinees loess stratigraphic system (Kukla, 1987) but carry the prefix "SL", referring to the Stari Slankamen site.

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3. METHODS

A total of 59 oriented samples was taken, spanning a stratigraphic thickness of 40 m. The analyses were conducted at the paleomagnetic Laboratory of the Institute of Geophisics at the ETH Zürich. The characteristic remanent magnetization (ChRNM) was obtained after alternating field (AF) demagnezation between 5 and 15 mT. MS variations of lower part of the profile (from the base to loess layer SL L5) measured in the field using a portable Bartington susceptibility meter. At each level, 10 indipendent readings were taken and averaged. Samples from upper part of the exposure were measured in Lamont-Doherty Geophisical laboratory in Palisades on the Bartington probe MS2B with 36 mm opening at a frequency of 0.47 kHz. Selected samples from lower part of profile were also remeasured, which made it possible to normalize susceptibility values obtained by different instruments. Measurements level in the field and samples sites were at 10 cm intervals in paleopedological horizon and at 15 cm intervals in loess layers.

4. MAGNETIC REVERSALS

The most important point in the chonological division of the Stari Slankamen exposure is the occurrence of the Matuyama-Bruhnes poleomagnetic chrons boundary (MBB) (0.78 Ma; Cande and Kent, 1995). The ChRM data obtained after AF demagnetization give clear evidence of MBB position at depths of 36 m in lower part loess layer SL L8 (fig. 3). Transitional magnetic polarity interval is visible below to MBB. This is the first observation of MBB in loess-paleosol sequences of Serbia.

5. MAGNETIC SUSCEPTIBILITY

Low field MS variations in the Stari Slankamen loess-paleosol sequence well reflected Middle and Late Pleistocene paleoclimatic fluctuations. MS values, in general, decreased during the time. High MS values are observed in paleosols (average 6.85 x 10^{-7 m3 kg-1) are in average more than twice as high as in the loess units (average 3.17 x 10-7 m3 kg-1) (fig. 3). The lowest MS value was measured in loess unit SL L2 (1.03 x 10-7 m3 kg-1) and the highest value is detected in paleosl SL S7 SS2 (16.57 x 10-7 m3 kg-1).}

This type of MS cyclicity reflects magnetic enhancement via pedogenesis and is similar to that in Chinese and Central Asian loess deposits (e.g. Maher and Thomson, 1999). General decreasing of MS values during the time clearly support Bronger’s (1976) paleoclimatic reconstruction based on paleopedological data.

6. CHRONOSTRATIGRAPHY REVISION

Data in Tab. 1 summarized existing chonostarphic models of the Stari Slankamen loess-paleosol sequences. Bronger (1976) correlated paleosols from F2 to F4 with period of Würm glacial and paleosol F5 with Riß-Würm interglacial. TL dates of Stari Slankamen loess-paleosol sequences indicate that fossil chernozems F2 and F3 have been formed during MIS 5a and 5e (Singhvi et al., 1989). Bronger and Heinkele (1989) suggested that the most strongly developed palesol F6 at Stari Slankamen is related to Chinese pedocomplex S5 and both MIS 13 and 15. According to Butrym et al. (1991) the youngest paleosols (F2-F4) are time equivalents of MIS 5a, 5c and 5e, fossil soil F4 has been developed during the MIS 7 and F5 and F6 have been formed at the time of MIS 9.

This type of MS cyclicity reflects magnetic enhancement via pedogenesis and is similar to that in Chinese and Central Asian loess deposits (e.g. Maher and Thomson, 1999). General decreasing of MS values during the time clearly support Bronger’s (1976) paleoclimatic reconstruction based on paleopedological data.

6. CHRONOSTRATIGRAPHY REVISION

Data in Tab. 1 summarized existing chonostarphic models of the Stari Slankamen loess-paleosol sequences. Bronger (1976) correlated paleosols from F2 to F4 with period of Würm glacial and paleosol F5 with Riß-Würm interglacial. TL dates of Stari Slankamen loess-paleosol sequences indicate that fossil chernozems F2 and F3 have been formed during MIS 5a and 5e (Singhvi et al., 1989). Bronger and Heinkele (1989) suggested that the most strongly developed palesol F6 at Stari Slankamen is related to Chinese pedocomplex S5 and both MIS 13 and 15. According to Butrym et al. (1991) the youngest paleosols (F2-F4) are time equivalents of MIS 5a, 5c and 5e, fossil soil F4 has been developed during the MIS 7 and F5 and F6 have been formed at the time of MIS 9.

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Magnetostratigraphic data presented in this study suggest serious revision of previous age determinations of Stari Slankamen loess-paleosl sequences. MS variations in the upper part of profile suggest point to correlation of paleosols SL S1, SL S3 and SL S4 with MIS 5, 9 and 11. This chronostratigraphic interpretation confirms previous opinion that strongly developed paleosol SL S5 was formed during the MIS 13-15. This noticeable pedocomplex is sharply visible in the middle part of all Euroasian Brunhes loess-paleosol columns (Bronger, 2003). Paleosol SL S6 is probable formed during the MIS 17. However, lower part of Stari Slankamen exposure show different paleoclimatic and paleoenvironmental image. More humide conditions caused pedogenesis of thin paleosols SL L7 SS1, Sl S7 SS1 and Sl S7 SS2 which would be equivalents to MIS 18.3, 19.1 and 19.3.

Table 1 Chronostratigraphic models of the Stari Slankamen loess-paleosol sequence

Bronger (1976)

Singhvi et al. (1989)

Bronger & Heinkele (1989)

Butrym et al. (1991)

Our model

lithology

Alpine sudivision

MIS

MIS

MIS

lithology

MIS

F2

Würm paleosols W

5a

5a

5а

SL S1

5

F3

5e

5e

5c

Not observed

F4

5e

SL S3

9

F5

R-W

9 or 11

7

SL S4

11

F6

13-15

9

SL S5

13-15

F7

9

SL S6

17

F8

SL 7SS1

18,3

F9

SLS7SS1

19,1

F10

SLS7SS2

19,3

F11

SL S8

21

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7. CORRELATION WITH KEY DANUBE LOESS SITES

The correlation between Stari Slankamen sequence and key Danubean loess-paleosol sites is based on: BBM position, relation among main MS peaks, earlier pedostratigrapy investigations (Bronger, 1976, 2003; Bronger and Heinkele,1989; Bronger et al., 1998) and the well established age according to luminescence dating and AAR geochronology (Singhvi et al., 1989; Zöller et al., 1994; Oches and McCoy, 1995a, 1995b).

Figure 3 Correlation between glacial cycles according Kukla (1975), chronostraigraphy of deep see site ODP 677 (Shackleton et al., 1990) and magnetostraphy models of key loess sites in Danube loess area Paks (Sartori et al., 1999), Stari Slankamen, Koriten (Jordanova and Petersen, 2001) and Novaya Etuliya (Tsatskin et al., 2001)

Figure 3 shows correlation between deep sea oxygene stratigraphy (Shackleton et al., 1990), glacial cycles (Kukla, 1975) and magnetostratigraphic models of main sections in loess Danube loess area: Paks in Hungary (Sartori et al., 1999), Stari Slankamen, Koriten in Bulgaria (Jordanova & Petersen, 2001) and Novaya Etululiya in Ukraina (Tsatskin et al., 2001). This correlation complete previous interpretation of Central European loess stratigraphy based on investigations of Czech and Austrian exposures: Červeny Kopec, Krems & Stanzendorf (Kukla, 1975; Kukla & Cilek, 1996)

8. CONCLUSIONS

Stari Slankamen is the first Serbian loess site with detalied magneto-stratigraphical record. Paleomagnetic measurements of the Stari Slankamen loess-paleosol sequence provide a evidence of BBM position in the lower part of the oldest loess horizon SL L8. Chonostratigraphic model presented in this study suggest mostly downwards revision of previous age determinations. The new chronological scheme matches well with MIS despite strong influence of Middle Pleistocene paleoclimatic transition to loess-paleosol sequences deposition.

10Milutin Milankovitch Anniversary Symposium Field Guide Book

Our results confirm Stari Slankamen loess-paleosl sequence as one of the most important site for reconstruction of Middle Pleistocene paleoclimate in this part of Europe.

9. REFERENCES

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12Milutin Milankovitch Anniversary Symposium Field Guide Book

THE FIRST SCIENTIFIC DESCRIPTION OF EUROPEAN LOESS-PALEOSOL SEQUENCES

Marković B. Slobodan & Јovanović Мladjen

Quaternary research centre, University of Novi Sad, Trg D. Obradovića 3, 21000 Novi Sad, Serbia and Montenegro

This short communication highlights importance of our excursion area to loess research in Europe, beginning with the work of Luigi Ferdinando Marsigli (figure 1).

During the last decade of 17^{th century Marsigli was employed to arrange the boundaries between the Turkey, and Austrian Empire. As high officer of Austrian army Marsigli spent a lot of time in Patrovaradin, Titel and Stari Slankamen forts. Italian soldier and scientist, at the same time worked on his military duties and also investigated loess-paleosol exposures situated close to these fortifications. Noticeable loess-paleosol exposures along Danube river valley have been drawn by Marsigli in his outstanding six volume book Danubius Pannonico Mysicus (1726). Cont Marsigly described lithology of loess bank of Danube river, respectively, modern soil (marked with A in Figure 1) as Terra fructifera pinguis nigra et creatacea (black fertile carbonate soil), paleosol (B) as Terra nigra fructifera pinguis (black fertile soil) and between them loess layer (C) as Terra lutosa cinerive et in fragmento creatacea priabilis [yellow-cinerary layer with carbonate fragments (concretions)] (figure 2). To summarize, it is evident that many sedimenthological characteristics of loess-paleosol sequences as recognized by Marsigli remain valid to this day.}

Marsigli’s observations of loess-paleosol sequences was published one century before pioneering work of von Leonard’s (1823/1824) about characterization of loess deposits (Zoeller & Semmel, 2001). Ever since the initial study of Marsigli loess research around the world have

13Milutin Milankovitch Anniversary Symposium Field Guide Book

been established as one of the most promising tools for understanding of Quaternary plaeoclimatic evolution.

REFERENCES

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NOVI SAD

Novi Sad arose on the left bank of the river Danube, in Backa. It spreads across the alluvial terrace and on the old Danube road, at the site of the most suitable approach to the Danube and most convenient crossing from Backa into Srem, where the Danube is only 350 m wide.

The city is connected with several settlements in the outskirts. It is one of the largest economic and cultural centres in Serbia and Montenegro. Novi Sad is the capital of the Autonomous Province of Vojvodina. It is divided in two municipalities: Novi Sad and Petrovaradin. Together with the outskirts settlements they have 304.519 inhabitants in total. The city is located between 19° 51' of the east longitude and 45° 20' of the north latitude. Today Novi Sad has a population of about 300,000 inhabitants and highly developed economic and cultural activities. The first Grammar School was founded in 1810. The first professional theatre – The Serbian National Theatre was founded 1861, and the oldest cultural distribution among the Serbs – the Matica srpska moved from Budapest to Novi Sad in 1864. What is now known as The Serbian Academy of Arts and Sciences – Novi Sad branch was the Academy of Arts and Sciences of Vojvodina founded in 1979.

UNIVERSITY OF NOVI SAD

http://www.ns.ac.yu/stara/eng/prezentacija.html

The University of Novi Sad is an educational, scientific and art institution founded by the Republic of Serbia. The activity, organization, management and financing of the University are all regulated by University Statutes. The University and the faculties of which it is comprised have educational and scientific autonomy.

Historical background

Educational activities in Vojvodina and Novi Sad have a tradition of more than a few hundred years: 11th century - Roman Catholic Latin school in Bač, 12th century - Roman Catholic Latin school in Titel. From the middle of the 16th century until the end of the 17th (the period of Turkish occupation) centres of nastery school in Hopovo, 1607 – Monastery school in Kovilj, 1621 – Monastery school in Bođani, 1687 – Roman Catholic monastery schools in Subotica and Sombor, 1606 – Serbian public school in Vršac, 1618 – Serbian public school in Veliki Bečkerek, 1703 – Schools in Petrovaradin and Sremska Kamenica, The Rumanians founded their first schools close to Orthodox churches, in 1736 in Veliko Središte, First Ruthenian schools were founded in 1753 in Ruski Krstur and in 1765 in Kucura, Oldest Slovakian schools were established in 1770 in Bački Petrovac, in 1780 in Gložan and in 1785 in Kisač, 1726 – Slavic Latin school in Sremski Karlovci, at the level of lower secondary school, 1794 – Serbian Orthodox Seminary in Sremski Karlovci, training priests and teachers, 1791 – First Serbian grammar school – »Gymnasium« in Sremski Karlovci 1778 – Teacher Training school in Sombor, developed from the courses given by Avram Mrazović, 1810 – Serbian Orthodox Grammar School in Novi Sad, 1881 – Women's teacher training school in Subotica,

learning were founded, as follows: 1573 – Mo 15

1881 – Lower school for tradesmen and merchants in Novi Sad, 1885 – School of commerce in Sombor, 1895 – School of commerce in Veliki Bečkerek, 1906 – School of commerce in Subotica, 1920 – Faculty of Law in Subotica, 1947 – Teachers’ college in Novi Sad, 1954 – First faculties in Novi Sad were opened.

Founding of the University

The University of Novi Sad was founded on June 28, 1960. and it represents an autonomous institution for education, science and arts. The University is comprised of 13 faculties located in the four major cities of the autonomous Province of Vojvodina: Novi Sad , Subotica, Zrenjanin, Sombor.

Symposium Field Guide Book 16

Location of the University

The University is situated on the University campus (totals 259,807 square meters) on the left bank of the Danube river near Novi Sad's city centre. In addition to the administrative building, the university campus comprises the faculties, the Student centre with two Student Dormitories and the Central Student Cafeteria, an Apartment Hotel for temporary accommodation of young teaching fellows and research assistants, the Student health centre and the Centre for Physical Education.

There are also many other scientific, professional, cultural, information, sports and similar student organizations. The student square on the University campus adds to the attractive surroundings.

Out of 13 faculties of the University of Novi Sad, 9 are seated in Novi Sad. Seven of them operate in modern buildings built on the University Campus: the Faculty of Letters and Humanities, the Faculty of Agriculture, the Faculty of Technology, the Faculty of Law, the Faculty of Engineering, the Faculty of Natural Sciences and Mathematics and the Faculty of Physical Education. The Faculty of Medicine is located on the grounds of the Clinical Center, while the Academy of Arts is housed partially in the immediate city center and partially in the Petrovaradin Fortress.

Milutin Milankovitch Anniversary Symposium Field Guide Book

Four faculties are situated elsewhere: The Faculties of Economics and Civil Engineering are in Subotica, the "Mihajlo Pupin" Faculty of Technical Engineering is in Zrenjanin, and the Teacher's Training Faculty is in Sombor.

Organization and Management of the University

Besides the faculties that comprise the University, the structure of the internal organization consists of: 1) The Rector's Office 2) Secretariat 3) ACIMSI – Association Center for Interdisciplinary and Multidisciplinary Studies and Research 4) International office 5) Central Library 6) ARMUS - Academic Computer Network

The University administrative bodies are: the Rector and the University Council. The professional University body is the Teaching and Research Council with its auxiliary expert organs: The Expert Councils for interdisciplinary and multidisciplinary studies and commissions and boards for specific questions concerning educational and scientific activity.

The Rector convenes the Collegium of the University, a consulting body for surveying questions and making policy decisions within the range of the Rector's responsibility, and for developing mutual cooperation and coordination among the faculties. The Collegium consists of the Rector, Vice-Rectors, Secretary General and the Deans of all of the faculties comprising the University.

Expert positions at the University are filled by officers employed in the Expert Offices.

Professors, Teaching Associates and Researchers

Teaching at the University and at the faculties is entrusted to professors and teaching associates who hold academic titles prescribed by law. Scientific and artistic activities are taught by researchers and art associatesholding corresponding titles prescribed by law. The University monitors the advancement of its professorial staff and takes measures for their further advancement. It participates in the procedure for awarding doctorate degrees at the faculties and take measures for improving the financial status of professors, teaching associates and researchers. The University confers doctorates in interdisciplinary and multidisciplinary fields, and honorary doctorates. The Rector of the University officially confers the doctorate degree on candidates who have acquired their doctorates at the University and its faculties.

The University devotes special attention to young lectures and researchers. To create the best possible conditions for their work and development, the University provides temporary housing for about 150 young lecturers and scientists, together with their families, in two halls of residence built specifically for them.

17Milutin Milankovitch Anniversary Symposium Field Guide Book

MILANKOVITCH’S MONUMENT AT UNIVERSITY CAMPUS IN NOVI SAD

The bust of Milutin Milankovitch monument made by Vladimir Jokanović is positioned in front of the building of Departments for Physics and Mathematics.

Figure 1. Milankovitch’s monument at University campus (Photo: P. Antoine)

THE BRIDGE "SLOBODA"

www.vojvodina.com

The President of the Society of the civil engineering constructors of Vojvodina, engineer Ivan Mamuzic, who is also the President of The Society of engineers and technicans of Novi Sad, was the main supervising engineer during the building of the Bridge of Freedom in Novi Sad, designed by theAcademy member, professor dr Nikola Hajdin.

The bridge, which was rightfully thought of as the most beautiful on the Danube, took nearly ten years to be completed. The scientific study of the river bed of the Danube was completed in 1972.; in 1976. construction works were oficially started placing the first

18Milutin Milankovitch Anniversary Symposium Field Guide Book

foundation pillar on the left river bank. On October 23rd 1981. the bridge was finally put into function. Today, there is no bridge any more, says engineer Mamuzic.

The bridge was 1,312 metres long, supported by 23 pillars, only three of which are in the water. It had six lanes 27.68 metres wide as well as and two sidewalks. 27,000 cubic metres of concrete were built into the bridge; the main steel structure was 591metres long and weighed 7,600 tons. Main contractor was "Mostogradnja" from Belgrade with it's subcontructors; the steel structure has been delivered by "Gane-Mavag" from Budapest, Hungary; steel ropes have been supplied through "Stahlton" A.G. from Zurich, Switzerland; two special large bearings of carrying capacity 10,000 tons were also imported.

Member of the Institute for civil engeneering planning in the municipality of Novi Sad, Mr. Zoran Obradovic, who took part in project planning and construction works of the bridge, says that construction works were in compliance with strict regulations (German DIN regulations), therefore the bridge provided even 60 tons heavy vehicle to pass, which is rarely possible in peace.

351 metre bridge span was the world record in the category of bridges with sloping tights in the middle. The bridge was hit by the missile in the root point of supporting pillar, the pillar situated on Novi Sad river bank fractured. On the other bank, the missile effect was not such fatal. The bridge lost carrying capacity of all ropes on the side facing Novi Sad; main support has suffered severe damages and it is now bent in Danube. Nevertheless, it will be possible to further use the majority of construction material, but the greatest problem is the process of drawing the material out of water. The preparation of special elaborate for such action will be necessary.

Bridge elements are 200 t heavy and have been previously composed applying special procedure. It will be more difficult to draw them out of water, as cranes' carrying capabilities do not exceed 100 tons. In case these elements are ment to be rebuilt, they must be carefully cut under water, which is very complicated procedure because of the influence of the river current. The engagement of divers and meny other professionals will be necessary, and the procedure may take months. There is no doubt that special project for drawing useful bridge elements out of water should be made.

The value of the bridge steel structure is being estimated to 50 million dollars US, and the value of the whole bridge is being estimated between 100 and 150 million dollars US.

19Milutin Milankovitch Anniversary Symposium Field Guide Book

VIEW 1

THE LATE PLEISTOCENE LOESS-PALEOSOL SEQUENCE MIŠELUK

Marković B. Slobodan ^{1, Oches A. Eric2, Gaudenyi Tivadar1, Jovanović Mladjen1, Hambach Urlich, Zöller Ludwig & Sümegi Pal3}

1 Quaternary Research Centre, University of Novi Sad, Trg Dositeja Obradovića 3, 21000 Novi Sad, Yugoslavia

2 Department of Geology, University of South Florida, 4202 Fowler Ave.-SCA 528, Tampa FL 33620, USA

3 Department of Geology and Paleontology, University of Szeged, Egyetem u. 2-6, H-6722, Szeged, Hungary

The Mišeluk section is situated between Petrovaradin and Sremska Kamenica on the right bank of Danube River, opposite to Novi Sad. In this part of north slope of Fruška gora Mountain loess covers a fossil landslide and mantles the Danube’s alluvial plane. Geographical coordinates of the Mišeluk site are 45o16` N Latitude and 19o52` E Longitude (Fig. 1). Approximately 7 m Mišeluk profile thickness includes recent and two fossil soils separated by three loess layers, which have been formed during the last about 145 ka.

Figure 1 Aminostratigraphy of the Mišeluk section compared with Central European localities for glacial cycles B and C, corresponding to marine oxygen-isotope stages 2-5 and 6-7, for the genera Trichia (A) and Pupilla (B)

Seven different genera of terrestrial gastropod shells have been analyzed, including samples from eight levels within the sequence of loess and paleosols at Mišeluk. Sampled genera include Chondrula, Clausilia, Ena, Granaria, Orcula, Pupilla and Trichia. Alloisoleucine/Isoleucine total acid hydrolysate (A/I–HYD) measurements on representative samples are shown in figure 1. Shells of the genus Puiplla and Trichia were the most abundant and offer the most direct aminostratigraphic comparison with data from loess units elsewhere in

1 Quaternary Research Centre, University of Novi Sad, Trg Dositeja Obradovića 3, 21000 Novi Sad, Yugoslavia

2 Department of Geology, University of South Florida, 4202 Fowler Ave.-SCA 528, Tampa FL 33620, USA

3 Department of Geology and Paleontology, University of Szeged, Egyetem u. 2-6, H-6722, Szeged, Hungary

The Mišeluk section is situated between Petrovaradin and Sremska Kamenica on the right bank of Danube River, opposite to Novi Sad. In this part of north slope of Fruška gora Mountain loess covers a fossil landslide and mantles the Danube’s alluvial plane. Geographical coordinates of the Mišeluk site are 45o16` N Latitude and 19o52` E Longitude (Fig. 1). Approximately 7 m Mišeluk profile thickness includes recent and two fossil soils separated by three loess layers, which have been formed during the last about 145 ka.

Figure 1 Aminostratigraphy of the Mišeluk section compared with Central European localities for glacial cycles B and C, corresponding to marine oxygen-isotope stages 2-5 and 6-7, for the genera Trichia (A) and Pupilla (B)

Seven different genera of terrestrial gastropod shells have been analyzed, including samples from eight levels within the sequence of loess and paleosols at Mišeluk. Sampled genera include Chondrula, Clausilia, Ena, Granaria, Orcula, Pupilla and Trichia. Alloisoleucine/Isoleucine total acid hydrolysate (A/I–HYD) measurements on representative samples are shown in figure 1. Shells of the genus Puiplla and Trichia were the most abundant and offer the most direct aminostratigraphic comparison with data from loess units elsewhere in

20Milutin Milankovitch Anniversary Symposium Field Guide Book

central and eastern Europe. HYD A/l values measured in Puiplla and Trichia from the Mišeluk profile can be compared with data from Austrian, Czech, Slovakian, Hungarian and German sites (Oches & McCOY, 1995a, 1995b, 2001; Oches et al., 2000) (fig. 3). AAR geochronology results from Mišeluk sections support the previous chronostratigraphic scheme of Marković et al. (2000). According to that chronostratigraphic model, loess-paleosol sequences L1 and S1 formed during glacial cycle B (Kukla, 1975), correspond with Marine oxygen-isotope stages (MIS) 2, 3, 4 and 5. Uncovered part of L2 loess horizon is deposited during the youngest part of glacial cycle C and MIS 6.

Magnetic susceptibility record and sedimentological evidence supported a correlation with the SPECMAP paleoclimatic model (Marthinson et al., 1987) over the last about 140.000 years (figure 2).

Figure 2 Correlation between the magnetic susceptibility record of the Mišeluk loess-paleоsol sequence and SPECMAP δ^{18O series.}

The 32 specimens (17 families) of 3831 individuals of land snail fauna were found in 24 samples of the Mišeluk section. In generally, identified land malocological assemblage appear relative humid and cold paleonvironmental conditions. Figure 6. present distribution of some characteristic species in Mišeluk loess layers.

The snail assemblage from upper part (final stage) of the L2 horizon (5,35-6 m depth) is characterized by quite great number of shells per samples (more than 500 individuals per sample) with a dominance of humid places preferring species, of different biotopes. The presence of dominant species Trichia striolata, Vitrea crystallina Punctum pygmaeum, Aegopinella ressmanni and Clausilia dubia indicate existing of humid closed and open environment. The

The 32 specimens (17 families) of 3831 individuals of land snail fauna were found in 24 samples of the Mišeluk section. In generally, identified land malocological assemblage appear relative humid and cold paleonvironmental conditions. Figure 6. present distribution of some characteristic species in Mišeluk loess layers.

The snail assemblage from upper part (final stage) of the L2 horizon (5,35-6 m depth) is characterized by quite great number of shells per samples (more than 500 individuals per sample) with a dominance of humid places preferring species, of different biotopes. The presence of dominant species Trichia striolata, Vitrea crystallina Punctum pygmaeum, Aegopinella ressmanni and Clausilia dubia indicate existing of humid closed and open environment. The

21Milutin Milankovitch Anniversary Symposium Field Guide Book

closed, humid environment preferring species Ena montana and Discus ruderatus have been found with very low frequency in the rest of samples.

Malacological investigations showed no presence of land snails in palosol S1 (4,5-5,25 m depth) was not valuable for malacological investigations because the chemical and the bad conservation processes makes a horizon sterile (without fossil shells).

During the loess layer L1 deposition presence of of closed vegetation preferring species as Punctum pygmaeum, Aegopinella ressmanni and species of Clausilidae family but their number of individuas in decreasing in relation to L2 loess horizon. During the last glacial we could mark the presence of two colde stadials which indicated presence of Vallonia tenuilabris and Columella collumella. Increasing of total molusk number and presence of Granaria frumentum suggest a warmer period during deposition of middle part of L1. At the end of the last glacial cycle environment has been changed to the open character with drier weather condition.

The snail assemlage from both Mišeluk's loess layers shows more humid and relative colder environment than in other sites in the south-east part of Charpatian (Pannonian) basin. The Mišeluk loess site has an important role during the late Pleistocene. It has a kind of refugial area, it is one of those rare places on the South-east part of Carpathian Basin where the Palaeopreillyrian snail assemblage (Sumegi, 1996) survived (Macrogastra ventricosa, Aegopinella ressmanni and Trichia edentula).

Figure 3 Characteristic land snail species in Mišeluk loess exposure

1. Hygrophilous, closed environment preferring specie; 2. Cold tolerant, hygrophilous species preferring open habitats; 3. Highly tolerant, sub hygrophilous species living in zones transitional between open and closed vegetation; 4. Highly tolerant, mesophilous species. living in zones transitional between open and closed vegetation; 5. Highly tolerant, mesophilous species. living in open areas; 6. Frigophilous, aridity tolerant species preferring open habitats; 7. Xerophilous, warm-loving species preferring open habitats.

Investigations of Mišeluk's loess-paleosol sequences during the last several years have established the importance of this site as a record of late Pleistocene paleoclimate and paleoenvironment in southeastern part of Carpathian (Pannoian) basin. The amino acid dating of

22Milutin Milankovitch Anniversary Symposium Field Guide Book

loess-paleosol sequences in this region confirm stratigraphic and temporal correlations with other central European sites.

Fossil gastropod fauna from the loess and paleosols at Mišeluk provide additional important paleoenvironmental information. Establish fossil land snail assemblages preserved in loess also indicate the dominance of hygrophilous and shade loving species which suggest a relative humid paleoclimate compared to conditions interpreted from loess sediments elsewhere in the southern-eastern part of Carpathian (Pannonian) basin. Malacofauna of Mišeluk site included species as Aegopinella ressmanni, Macrogastra ventricosa and Ena montana in loess below and above paleosol S1, it demonstrates a significant similarities to Paleopreilyrian refugial fauna of south Transdanubia region in Hungary, which suggest that Mišeluk has a refugial character during the periods of loess accumulation.

REFERENCES

23Milutin Milankovitch Anniversary Symposium Field Guide Book

STOP 3

PETROVARADIN FORTREES

http://www.novisadtourism.com

PETROVARADIN FORTRESS AND ITS SECRETS

Today Petrovaradin Fortress is an integral part of the urban entirety of Novi Sad. The fortress was built according to the system Voban. It is among several remaining fortresses in the West and Central Europe that is almost totally preserved. "Gibraltar on the Danube" extends across 112 hectares, has four floors in the ground, more than 16 km of tunnels, around 12 000 loopholes and 13 gates.

HISTORY OF THE FORTRESS

Origin At the present place of the fortress, there used to be a medieval fortress built between 1247 and 1252, and before that one there were Celts, Romans, Huns, Avars. The Slavs and Avars settled the area in the VI and VII centuries. The new fortress was mentioned in written documents in 1347 for the first time as the residence of various commanders. According to the latest evidence of the archaeological research, the traces of human life on the fortress date back from Palaeolithic period. The Fortress was completed in 1780. Inaccessible for military equipment of that time, it occupied the dominant position in regard to the surroundings and became known as "The Gibraltar on the Danube".

The Influence of the Ottoman Empire

During history, the fortress changed masters and appearance, thus in 1526 the Turks occupied it, under the leadership of Sulejman II the Magnificent. They built a pontoon in order to cross the river more easily. While in war with Austria, the Turks left the Fortress several times but also returned when it had a Lower and Upper Town. In the suburb, there was Suleiman-han mosque as well as Muslim quarters, but also one Christian quarter. The Turks ruled the medieval Petrovaradin Fortress for 161 continually, from 1526 to 1689.

The Reconstruction of the Fortress

The Austrian Army conquered the Fortress in 1691 under the leadership of the Count Ludwig Badenski. According to the projects of the French military architect Sebastian Voban (who made projects for about 60 fortresses in Europe), the Austrian military engineers started building a completely new fortress in 1692. The new Voban’s system of fortification implied lower walls, i.e. bastions and ramparts, since the construction had to adjust to the plain area – spreading spatially and entering the bowels of Petrovaradin Fortress with underground passages. Besides German workers, who were paid for their work, the other workers in the construction of the fortress were mostly vassals, convicts and prisoners of war. The construction was stopped in 1694 because of the Turkish attack, but it never became theirs again since they retrieved towards Belgrade due to the lack of food and cholera epidemic. The memory of that event is engraved on the portal of the Eastern Gate that leads towards the Upper Town. The Austrians built a triangular bridgehead the same year, which was the beginning of Novi Sad. The present church at Tekije was built in 1881 as a memory of the great victory of Christians over the Turks in 1716. It was built to honour Blessed Virgin Mary, who according to the legend came to the present Austrian army commander’s dream and told him about the victory.

Settling the Fortress

Civil population started settling the foothill after 1702. There were around 50 town houses built in baroque style where Catholics, mostly Germans lived. Non-Catholics could not get a house nor the citizen’s rights here. That is why the Serbs, Jews, Cincars and other nations

24Milutin Milankovitch Anniversary Symposium Field Guide Book

crossed the river and created a settlement, predecessor of the present Novi Sad. Adaptation, restoration and conservation of the facilities at the Fortress started in 1951 because it stopped serving as a military center in 1948. Along St. Teresa Bastion, i.e. Empress Maria Theresa’s Bastion, on the ground floor of the Long Barracks, in the shadows of the ash treetops, a line of ateliers of Novi Sad fine and applied art artists are arranged. These rooms (besides barber’s shop and timber yard) were once used for technical services and craft workshops: boot makers, shoemakers, tailors, saddlers, gunsmiths, locksmiths, carpenters, builders, blacksmiths, wheelwrights, etc. The members of the Painting Circle work here today. Ateliers are often open for public when the artists are there. The Museum of the Town of Novi Sad, The Historical Archive and Hotel "Varadin" are located on the upper Fortress.

Figure 1 Petrovaradin fortress (photo S. Marković)

25Milutin Milankovitch Anniversary Symposium Field Guide Book

VIEW 2

THE LATE PLEISTOCENE LOESS-PALEOSOL SEQENCES AT PETROVARADIN BRICKYARD EXPOSURE (VOJVODINA; SERBIA)

Marković B. Slobodan^{1, Oches A. Eric2, Zöller Ludwig 3, Savić Stevan 1, Gaudenyi Tivadar1, Jovanović Mladjen1, Sümegi Pal4, McCoy D. William5 & Ivanisević Petar 6}

1Quaternary Research Centre, University of Novi Sad, Trg Dositeja Obradovica 3, 21000 Novi Sad

2Department of Geology, University of South Florida, 4202 E. Fowler Ave. SCA 528, Tampa FL 33620, USA

3Department of Geomorphology, University of Bayreuth, Universität str. 30, Bayreuth 95440, Germany

4Department of Geology and Paleontology, University of Szeged, Egyetem u. 2-6, H-6722 Szeged, Hungary

5Department of Geosciences, University of Massachusetts, Amherst, MA, 01003 USA

5Poplar Institute, Laboratory for Soil Science, University of Novi Sad, 21000 Novi Sad

Petrovaradin brickyard loess exposure is situated in the central part of the north slope of Fruška Gora Mountain (Vojvodina, Serbia). Geographical coordinates of this site are 45o 16’ N Latitude and 19o 52’ E Longitude. Initial investigations are focused on the both four loess layers and three paleosols preserved in the 8 m thick exposure of Petrovaradin brickyard.

Amino acid racemization geochronology provide correlations between loess-paleosol units at Irig brickyard with glacial cycles (Kukla, 1975) B and the youngest part of C, respectively, at other European localities (Oches et al, 2000; Oches & McCoy, 2001) (figure 1).

Figure 1 Aminostratigraphy of the Petrovaradin section compared with Hungarian (H), Slovakian (SK), Austrian (A), Czech (CZ) and German (D) localities for glacial cycles B, and C, corresponding to marine oxygen-isotope stages 2-5 and 6-7 for the genus Trichia.

Magnetic susceptibility, grain-size and carbonate content records, combined with malacological evidence, indicate many episodes of cold-dry and warm-wet paaleoclimatic conditions (figure 2).

1Quaternary Research Centre, University of Novi Sad, Trg Dositeja Obradovica 3, 21000 Novi Sad

2Department of Geology, University of South Florida, 4202 E. Fowler Ave. SCA 528, Tampa FL 33620, USA

3Department of Geomorphology, University of Bayreuth, Universität str. 30, Bayreuth 95440, Germany

4Department of Geology and Paleontology, University of Szeged, Egyetem u. 2-6, H-6722 Szeged, Hungary

5Department of Geosciences, University of Massachusetts, Amherst, MA, 01003 USA

5Poplar Institute, Laboratory for Soil Science, University of Novi Sad, 21000 Novi Sad

Petrovaradin brickyard loess exposure is situated in the central part of the north slope of Fruška Gora Mountain (Vojvodina, Serbia). Geographical coordinates of this site are 45o 16’ N Latitude and 19o 52’ E Longitude. Initial investigations are focused on the both four loess layers and three paleosols preserved in the 8 m thick exposure of Petrovaradin brickyard.

Amino acid racemization geochronology provide correlations between loess-paleosol units at Irig brickyard with glacial cycles (Kukla, 1975) B and the youngest part of C, respectively, at other European localities (Oches et al, 2000; Oches & McCoy, 2001) (figure 1).

Figure 1 Aminostratigraphy of the Petrovaradin section compared with Hungarian (H), Slovakian (SK), Austrian (A), Czech (CZ) and German (D) localities for glacial cycles B, and C, corresponding to marine oxygen-isotope stages 2-5 and 6-7 for the genus Trichia.

Magnetic susceptibility, grain-size and carbonate content records, combined with malacological evidence, indicate many episodes of cold-dry and warm-wet paaleoclimatic conditions (figure 2).

26Milutin Milankovitch Anniversary Symposium Field Guide Book

Figure 2 Paleoenvironmental and paleoclimatic record of loess-paleosol sequences at Petrovaradin brickyard site

The 33 specimens (26 families) of 5053 individuals of land snail fauna were found in 30 samples of the Petrovaradin section. Results of Malacofauna investigations of Petrovaradin site demonstrates significant similarities to the Paleopreilyrian fauna of the south Transdanubia region in Hungary, which suggests that has a refugial character during the periods of loess accumulation. Generally, identified land malocological assemblage appeared relative humid and cold paleonvironmental conditions. During the last glacial period total snail abundance increased in the contrast of decreasing of frequency of aridity tolerant species (figure 2).

During excavation of raw materials in to abandon, only 500 m far, mine of local brickyard in 1978, workers founded skeleton fragments of a wooly mammoth skeleton (Mammuthus primigenius) at the base of SL L1 loess (at depth 4.7 m from the top) (Milić, 1978), adding to the paleoecological picture of Mišeluk's upper Pleistocene environment.

REFERENCES

27Milutin Milankovitch Anniversary Symposium Field Guide Book

STOP 4

MONASTERY NOVO HOPOVO

htttp:www.ns.ac.yu/manastiri

Monastery Novo Hopovo (New Hopovo) is situated in central part of the north slopes of Fruška Gora Mountain, 5 km northeastern of town of Irig. This is one of the oldest monasteries in the Fruška Gora Monasteries group: the first trustful written resource with the mention of the Monastery dates from 1451 but at new archeological excavations was discovered existence of much older church structure on the same place. In vicinity, deep in forest, is small, very romantic, abounded Monastery of StaroHopovo (Old Hopovo) erected in late XV century by despot (duke) Djordje Branovic. Small church that there exist now is from 1751.

Figure 1 Monastery Novo Hopovo

Church that exists nowdays was built in 1575/76. with the financial donations of the group of wealthy citizens, especially Lacko and Marko Jovšić, from Kovin. The data concerning the church that precedes this one is insufficient. The existing church represents one of the biggest and one of the architectonically most valuable sacral buildings of its time. Its architectonical structure represents a unique mixture of different architectonic styles. The Novo Hopovo church made a strong influence on later builders of Fruska Gora monasteries. Monastery was always strong cultural center and one of the most famous monks who lived there was Dositej Obradović, great traveler, writer and educator.

28Milutin Milankovitch Anniversary Symposium Field Guide Book

VIEW 3

LATE PLEISTOCENE PALEOCLIMATE AND PALEOENVIRONMENT RECORDED IN THE LOESS-PALEOSOL SEQENCE AT IRIG BRICKYARD EXPOSURE (VOJVODINA; SERBIA)

Marković B. Slobodan^{1, Oches A. Eric 2, Gaudenyi Tivadar1, Jovanović Mladjen1, McCoy D. William3, Stevens Thomas3 Sümegi Pál4, Savić Stevan1, Ivanišević Petar5, Richard Walther2 & Zoran Galović5}

1Quaternary Research Centre, University of Novi Sad, Trg Dositeja Obradovica 3, 21000 Novi Sad, Serbia and Montenegro; zbir@im.ns.ac.yu

2Department of Geology, University of South Florida, 4202 E. Fowler Ave. SCA 528, Tampa FL 33620, USA

3Department of Geosciences, University of Massachusetts, Amherst, MA, 01003 USA

4Department of Geology and Paleontology, University of Szeged, Egyetem u. 2-6, H-6722 Szeged, Hungary

5Poplar Institut, Department of Soil science, Antona Čehova 13, 21000 Novi Sad, Serbia and Montenegro

The Irig brickyard loess exposure (45o 05’ N, 19o 52’ E) is situated in the central part of the south slope of Fruška Gora (Vojvodina, Serbia). Initial investigations are focused on the both four loess layers and three paleosols preserved in the 7 m thick exposure.

Amino acid racemization and luminescence geochronology provide correlations between loess-paleosol units at Irig brickyard with glacial cycles (Kukla, 1975) B and the youngest part of C, respectively, at other European localities (figure 1). Magnetic susceptibility, grain size and carbonate content records supported a correlation with the SPECMAP paleoclimatic model (Marthinson et al., 1987) over the last about 140.000 years (figure 2).

Figure 1 Aminostratigraphy of the Irig section compared with Hungarian (H), Slovakian (SK), Austrian (A), Czech (CZ) and German (D) localities for glacial cycles B, and C, corresponding to marine oxygen-isotope stages 2-5 and 6-7 for the genus Pupilla.

1Quaternary Research Centre, University of Novi Sad, Trg Dositeja Obradovica 3, 21000 Novi Sad, Serbia and Montenegro; zbir@im.ns.ac.yu

2Department of Geology, University of South Florida, 4202 E. Fowler Ave. SCA 528, Tampa FL 33620, USA

3Department of Geosciences, University of Massachusetts, Amherst, MA, 01003 USA

4Department of Geology and Paleontology, University of Szeged, Egyetem u. 2-6, H-6722 Szeged, Hungary

5Poplar Institut, Department of Soil science, Antona Čehova 13, 21000 Novi Sad, Serbia and Montenegro

The Irig brickyard loess exposure (45o 05’ N, 19o 52’ E) is situated in the central part of the south slope of Fruška Gora (Vojvodina, Serbia). Initial investigations are focused on the both four loess layers and three paleosols preserved in the 7 m thick exposure.

Amino acid racemization and luminescence geochronology provide correlations between loess-paleosol units at Irig brickyard with glacial cycles (Kukla, 1975) B and the youngest part of C, respectively, at other European localities (figure 1). Magnetic susceptibility, grain size and carbonate content records supported a correlation with the SPECMAP paleoclimatic model (Marthinson et al., 1987) over the last about 140.000 years (figure 2).

Figure 1 Aminostratigraphy of the Irig section compared with Hungarian (H), Slovakian (SK), Austrian (A), Czech (CZ) and German (D) localities for glacial cycles B, and C, corresponding to marine oxygen-isotope stages 2-5 and 6-7 for the genus Pupilla.

29Milutin Milankovitch Anniversary Symposium Field Guide Book

Figure 2 Correlation between the clay record of the Irig loess-paleоsol sequence and SPECMAP δ^{18O series.}

The relativly poor snail assemblage with dominant species such as Chondrula tridens, Granaria frumentum, Helicopsis striata and Pupilla triplicata suggest arid and relativly warm paleoclimatic conditions. The composition of mollusc fauna suggest that this region, parts of the southern slope of Fruska Gora mountain range, was a refugium for warm-loving and xerophilus mollusc taxa, where these elements could survive during the unfavourable climate periods of the Late Pleistocene. This is reflected in the continuous presence of Granaria frumentum specimens in the loess samples (figure 3).

Sedimentological, pedological, and paleontological evidence recorded in the Irig loess-paleosol sequence, all suggest periods of drier environmental conditions in this region than in other parts of the Pannonian (Carpathian) basin during the last ca. 140,000 years. The southern slope of Fruska Gora mountain was a biogeographical "island" during the last glacial, where a temperate grassland with dry-tolerant and warm–loving fauna elements remained even in the cold stages of the Late Pleistocene.

The relativly poor snail assemblage with dominant species such as Chondrula tridens, Granaria frumentum, Helicopsis striata and Pupilla triplicata suggest arid and relativly warm paleoclimatic conditions. The composition of mollusc fauna suggest that this region, parts of the southern slope of Fruska Gora mountain range, was a refugium for warm-loving and xerophilus mollusc taxa, where these elements could survive during the unfavourable climate periods of the Late Pleistocene. This is reflected in the continuous presence of Granaria frumentum specimens in the loess samples (figure 3).

Sedimentological, pedological, and paleontological evidence recorded in the Irig loess-paleosol sequence, all suggest periods of drier environmental conditions in this region than in other parts of the Pannonian (Carpathian) basin during the last ca. 140,000 years. The southern slope of Fruska Gora mountain was a biogeographical "island" during the last glacial, where a temperate grassland with dry-tolerant and warm–loving fauna elements remained even in the cold stages of the Late Pleistocene.

30Milutin Milankovitch Anniversary Symposium Field Guide Book

Figure 3 Characteristic land snail species in Irig loess exposure

1. Hygrophilus, temperate, closed vegetation preferring species; 2. Highly tolerant, subhygrophilous species living in zone transitional between open and closed vegetation; 3. Highly tolerant, mesophilous species living in zone trasitional between open and closed vegetation; 4. Highly tolerant, mesophilous species living in open areas; 5. Mildness preferring, aridity tolerant, open habitat (steppe); 6. Xerophilous, warm-loving species preferring open habitats.

REFERENCES

31Milutin Milankovitch Anniversary Symposium Field Guide Book

STOP 5

THE MIDDLE AND UPPER PLEISTOCENE LOESS-PALEOSOL SEQUENCE AT RUMA BRICKYARD, VOJVODINA, SERBIA

Marković B. Slobodan^{1, Oches A. Eric2, Jovanović Mladjen1 Gaudenyi Tivadar.1, Kostić Nikola3 & Sümegi Pal4}

1 Quaternary research centre, University of Novi Sad, Trg Dositeja Obradovića 3, 21000 Novi Sad, Serbia and Montenegro *corresponding author: fax + 381 21 468 244; e-mail zbir@im.ns.ac.yu

2 Department of Geology, University of South Florida, 4202 Fowler Ave.-SCA 528, Tampa FL 33620, USA

3 Department of Geology and Paleontology, University of Szeged, Egyetem u. 2-6, H-6722, Szeged, Hungary

1. INTRODUCTION

The Ruma loess-paleosol section is exposed in an excavation of a local brick factory on the left bank of Jelence Stream in the central part of the south slope of Fruška Gora. Geographical coordinates of this site are 45o00` N Latitude and 19o51` E Longitude (figure 1). The 20 m of thickness of the Ruma profile includes 5 fossil soils separated by 6 loess layers, which formed during the later part of the Middle and Late Pleistocene.

Figure 1 Topographic map of the area surrounding the Ruma brick mine

2. SAMPLING AND METHODS

Investigations of the loess-paleosol sequences of the Ruma quarry began in 1997. There are two exploitation levels of about 10 m thickness that were sampled in the northeast part of the quarry (fig. 2). Samples were collected at 5 cm intervals for sedimentological analysis, and at 25 cm intervals for malacological studies. Grain size fractions (<2, 2-10, 10-20, 20-200, >200 µm) were measured by sieving and pipeting and carbonate content was analyzed gas volumetrically. Magnetic susceptibility (MS): Measurements were done in the field using a portable Bartington

1 Quaternary research centre, University of Novi Sad, Trg Dositeja Obradovića 3, 21000 Novi Sad, Serbia and Montenegro *corresponding author: fax + 381 21 468 244; e-mail zbir@im.ns.ac.yu

2 Department of Geology, University of South Florida, 4202 Fowler Ave.-SCA 528, Tampa FL 33620, USA

3 Department of Geology and Paleontology, University of Szeged, Egyetem u. 2-6, H-6722, Szeged, Hungary

1. INTRODUCTION

The Ruma loess-paleosol section is exposed in an excavation of a local brick factory on the left bank of Jelence Stream in the central part of the south slope of Fruška Gora. Geographical coordinates of this site are 45o00` N Latitude and 19o51` E Longitude (figure 1). The 20 m of thickness of the Ruma profile includes 5 fossil soils separated by 6 loess layers, which formed during the later part of the Middle and Late Pleistocene.

Figure 1 Topographic map of the area surrounding the Ruma brick mine

2. SAMPLING AND METHODS

Investigations of the loess-paleosol sequences of the Ruma quarry began in 1997. There are two exploitation levels of about 10 m thickness that were sampled in the northeast part of the quarry (fig. 2). Samples were collected at 5 cm intervals for sedimentological analysis, and at 25 cm intervals for malacological studies. Grain size fractions (<2, 2-10, 10-20, 20-200, >200 µm) were measured by sieving and pipeting and carbonate content was analyzed gas volumetrically. Magnetic susceptibility (MS): Measurements were done in the field using a portable Bartington

32Milutin Milankovitch Anniversary Symposium Field Guide Book

susceptibility meter. MS was measured at 5 cm intervals; at each level, 10 independent readings were recorded and averaged. The mineralogical composition of bulk samples was obtained by X-ray diffraction of randomly oriented powder samples. Clay fractions (<2 ∝m) were separated by centrifugal sedimentation and analyzed mineralogically by X-ray diffraction with a SIMENS D-500 diffractometer using CuK〈 radiation and a 45-kV tube voltage. Oriented specimens were scanned over the 2–45^{o 2 ⎝range and step scanning at 0.02o 2Θmin. The DRX Win 1.4 software was used to quantify proportions of individual minerals in both the bulk samples and clay fractions. The hydrolytic alteration index of Thorez (1985) was calculated by multiplying the percent of each mineral in the clay fractions by its phase number: 7 for kaolinite, 5 for smectite, 3 for vermiculite, and so forth, then dividing the sum of these by the percentage of illite. The extent of mineral weathering was also estimated by comparing illite/(illite + quartz), and orthoclase/(orthoclase + quartz) ratios in the ground bulk samples. All data were analyzed statistically by the Statistica for Windows 4.3b package (Statsoft, 1996).}

10 kg bulk sediment samples were sieved through 0.7 mm mesh, and fossil gastropod shells were recovered and identified for paleoenvironmental interpretation. During the investigation from May 2000 to August 2001, several parts of bear skeletons (Ursus deningeri) were recovered from the SL L3 horizon. Preliminary preparation was done in the field by Gerhard Withalm and Hans Stutz from Institute of Paleontology, University of Vienna. The final conservation and paleontological interpretations will be completed at the Institute of Paleontology, University of Vienna.

Amino Acid Racemization (AAR) geochronology: Gastropod shells were collected from six loess layers and two paleosols for amino acid racemization analysis in order to independently correlate the stratigraphy at Vojvodina with loess-paleosol units elsewhere in Europe. Details of the sample preparation and analytical methodology are presented in Oches & McCoy (2001).

3. LITHO- AND PEDO-STRATIGRAPHY

Five paleosol and six loess layers are distinguished at the Ruma quarry (fig. 3). Although we provide a general overview here, details of paleosol stratigraphy and sedimentology are described by Marković et al. (2004). The two younger paleosol sequences show variable morphological characteristics. These soils were formed partly in paleo-depressions that are represented topographically as depressions in the present loess plateau surface (figure 2). Paleosol horizons developed in these paleo-depressions have greater thickness and darker color (Marković et al., 2000). These paleo-depressions are not noticeable in older fossil soil sequences.

Previous chronostratigraphic investigations of Serbian loess-paleosol sequences indicated that the loess horizons formed during glacial periods, and each paleosol developed during an interglacial phase (Marković, 2000, 2001). Based on these data, Marković and Kukla (1999) designated the units by names that follow the Chinese loess stratigraphic system (Kukla, 1987), beginning with the prefix "SL" referring to the standard section at the Stari Slankamen site.

Stratigraphy of the loess-paleosol sequence at Ruma is shown in figure 3. Only the uppermost part of SL L4, the oldest loess layer, is exposed. The oldest exposed paleosol, SL S3, is a strongly developed forest soil. From bottom to top, this paleosol complex includes a 105 cm thick C_{k horizon (10 YR 7/3-5/4, Munsell colors) with many carbonate concretions and strongly developed humus infiltrations; 25 cm thick BC horizon (10 YR 7/3-5/6) with small spherical carbonate nodules; 75 cm thick reddish Bt horizon, 10 YR 4/3 to 7.5 YR 3/2; with a 15 cm thick nearly indistinguishable elluvial layer at the top of the paleosol.}

10 kg bulk sediment samples were sieved through 0.7 mm mesh, and fossil gastropod shells were recovered and identified for paleoenvironmental interpretation. During the investigation from May 2000 to August 2001, several parts of bear skeletons (Ursus deningeri) were recovered from the SL L3 horizon. Preliminary preparation was done in the field by Gerhard Withalm and Hans Stutz from Institute of Paleontology, University of Vienna. The final conservation and paleontological interpretations will be completed at the Institute of Paleontology, University of Vienna.

Amino Acid Racemization (AAR) geochronology: Gastropod shells were collected from six loess layers and two paleosols for amino acid racemization analysis in order to independently correlate the stratigraphy at Vojvodina with loess-paleosol units elsewhere in Europe. Details of the sample preparation and analytical methodology are presented in Oches & McCoy (2001).

3. LITHO- AND PEDO-STRATIGRAPHY

Five paleosol and six loess layers are distinguished at the Ruma quarry (fig. 3). Although we provide a general overview here, details of paleosol stratigraphy and sedimentology are described by Marković et al. (2004). The two younger paleosol sequences show variable morphological characteristics. These soils were formed partly in paleo-depressions that are represented topographically as depressions in the present loess plateau surface (figure 2). Paleosol horizons developed in these paleo-depressions have greater thickness and darker color (Marković et al., 2000). These paleo-depressions are not noticeable in older fossil soil sequences.

Previous chronostratigraphic investigations of Serbian loess-paleosol sequences indicated that the loess horizons formed during glacial periods, and each paleosol developed during an interglacial phase (Marković, 2000, 2001). Based on these data, Marković and Kukla (1999) designated the units by names that follow the Chinese loess stratigraphic system (Kukla, 1987), beginning with the prefix "SL" referring to the standard section at the Stari Slankamen site.

Stratigraphy of the loess-paleosol sequence at Ruma is shown in figure 3. Only the uppermost part of SL L4, the oldest loess layer, is exposed. The oldest exposed paleosol, SL S3, is a strongly developed forest soil. From bottom to top, this paleosol complex includes a 105 cm thick C_{k horizon (10 YR 7/3-5/4, Munsell colors) with many carbonate concretions and strongly developed humus infiltrations; 25 cm thick BC horizon (10 YR 7/3-5/6) with small spherical carbonate nodules; 75 cm thick reddish Bt horizon, 10 YR 4/3 to 7.5 YR 3/2; with a 15 cm thick nearly indistinguishable elluvial layer at the top of the paleosol.}

33Milutin Milankovitch Anniversary Symposium Field Guide Book

Figure 3 Detalied sketch of Ruma exposure: 1. loess; 2. steppe soil; 3. steppe-forest soil; 4. forest soil; 5. crotovinas; 6. concretions; 7. intensive humic infiltrations. Arrows indicatepositions of Mammuthus primigenius and Ursus deningeri skeletal finds (Marković et al., in press).

Loess layer SL L3 (2.5 Y 8/2 – 10 YR 6/3) is about 200 cm thick and is relatively homogeneous silt to fine sand. Overlying this loess is SL S2 SS2, a 115 cm thick chernozem-brown forest soil paleosol complex. The lower C_{k and B (10 YR 6/3-4/4) horizons are 50 and 25 cm thick, respectively. Crotovina are scattered throughout the upper lighter colored (10 YR 5/4-4/3) 40 cm thick AB horizon. Subunit SL S2 LL1 is 75 cm thick weathered loess separating the subsoils of S2. Above this thin loess is the 45 cm thick SL S2 SS1, a light brown (10 YR 6/3-4/4) weakly developed chernozem.}

Pale yellow (10 YR 7/4-5/3) loess layer SL L2 is 375 cm thick. At 100 cm above the base of this loess unit, a 5 cm thick, darker (10 YR 6/3-5/4) horizon with weak humification is observed in the section. Many carbonate concretions (1-2 cm diameter) and humus infiltrations are developed at the contact between the SL S1 soil complex and the underlying SL L2 loess. The average thickness of overlying fossil soil SL S1 is 75 cm, although in paleo-depressions it reaches approximate 350 cm. The Ah horizon shows very similar morphological characteristics to the SL S2 fossil soil. However, profiles in paleo-depressions show a much more composite structure. Profiles of SL S1 paleosol in paleo-depressions include different colored, superimposed, chernozem soil horizons: (1) basal Ah4 layer (10 YR 5/1-3/2) is about 85 cm thick; (2) Ah3 is 35 cm thick and lighter in color (10 YR 5/2-3/3); (3) 75 cm thick Ah2 subhorizon is slightly darker in color (10 YR 5/1-3/2) with prismatic structure; and (4) Ah1 is the uppermost chernozem subhorizon (10 YR 5/1-3-3) with few carbonate concretions. At the top of this palesol complex is developed a light yellowish brown (10 YR 6/2-3/3) A(h) horizon of loess syrosem.

Above the SL S1 paleosol is a 160 cm thick, porous, pale yellow (2.5 Y8/4-5Y 6/4) loess, SL L1 LL2, with many modern bird holes, reflecting its sandier texture. The youngest fossil soil

Pale yellow (10 YR 7/4-5/3) loess layer SL L2 is 375 cm thick. At 100 cm above the base of this loess unit, a 5 cm thick, darker (10 YR 6/3-5/4) horizon with weak humification is observed in the section. Many carbonate concretions (1-2 cm diameter) and humus infiltrations are developed at the contact between the SL S1 soil complex and the underlying SL L2 loess. The average thickness of overlying fossil soil SL S1 is 75 cm, although in paleo-depressions it reaches approximate 350 cm. The Ah horizon shows very similar morphological characteristics to the SL S2 fossil soil. However, profiles in paleo-depressions show a much more composite structure. Profiles of SL S1 paleosol in paleo-depressions include different colored, superimposed, chernozem soil horizons: (1) basal Ah4 layer (10 YR 5/1-3/2) is about 85 cm thick; (2) Ah3 is 35 cm thick and lighter in color (10 YR 5/2-3/3); (3) 75 cm thick Ah2 subhorizon is slightly darker in color (10 YR 5/1-3/2) with prismatic structure; and (4) Ah1 is the uppermost chernozem subhorizon (10 YR 5/1-3-3) with few carbonate concretions. At the top of this palesol complex is developed a light yellowish brown (10 YR 6/2-3/3) A(h) horizon of loess syrosem.

Above the SL S1 paleosol is a 160 cm thick, porous, pale yellow (2.5 Y8/4-5Y 6/4) loess, SL L1 LL2, with many modern bird holes, reflecting its sandier texture. The youngest fossil soil

34Milutin Milankovitch Anniversary Symposium Field Guide Book

SL L1 SS1 (10 YR 6/3-4/3) is a weakly developed chernosem. Its thickness averages 45 cm, but increases to 105 cm in paleo-depressions. The last loess stratum, SL L1 LL1, is 175 cm thick, with characteristics similar to loess layer SL L1 LL2.

The Holocene soil developed in the loess plateau surface in the area surrounding Ruma is a calcareous chernozem (Živković et al., 1972). At the top of the investigated section the modern soil is light yellow-brown (10YR 6/3-4/4) and 55 cm thick, although in depressions it reaches a thickness of about 135 cm.

4. AMINO ACID GEOCHRONOLOGY AND CORRELATIONS

Amino acid racemization geochronology (AAR) has been successfully applied using fossil gastropod shells in the stratigraphic correlation of loess-paleosol sequences in different regions of the world (Oches & McCoy, 2001).

The Ruma profile is the first Serbian loess sequence in which AAR analyses have been carried out. Eight different genera of terrestrial gastropod shells have been analyzed, including samples from ten levels within the sequence of loess and paleosols at Ruma. Sampled genera include Bradybaena, Chondrula, Clausilia, Granaria, Helicopsis, Pupilla, Trichia and Vallonia. Alloisoleucine/Isoleucine total acid hydrolysate (A/I - HYD) measurements on representative samples are shown in figure 4. These data show a consistent increase in A/I values for individual genera from successively older stratigraphic units. Chondrula HYD A/I values increase from 0.08 ± 0.02 (n=5) in SL L1 to 0.19 ± 0.02 (n=4) in SL L2 to 0.24 ± 0.04 (n=2) in SL L3. However, based on initial data, A/I ratios are not able to distinguish between sub-horizons within a single stratigraphic unit. For example A/I data from SL-L1 LL1 and SL-L1 SS1 are indistinguishable; samples from upper and lower L2 show comparable values, and upper and lower SL L3 A/I ratios in Helicopsis overlap at one standard deviation (figure 4).

Shells of the genus Helicopsis, Trichia, and Pupilla are the most abundant and offer the most direct aminostratigraphic comparison with data from loess units elsewhere in central and eastern Europe. Trichia and Pupilla A/I values measured in samples collected from Ruma loess units are compared with data from across the European loess region (figure 5).

Figure 4 Positions of samples for amino acid analysis are shown as well as HYD A/I values for selected gastropod genera (Marković et al., in press).

35Milutin Milankovitch Anniversary Symposium Field Guide Book

Current mean annual temperatures in Serbia are higher than our other sampled localities (figure 5), and this gradient must be considered when establishing aminostratigraphic correlations. Based on these initial data from the Ruma loess section, we propose correlations between SL-L1 and loess of glacial cycle "B" elsewhere in Europe; SL-L2 correlates with cycle "C" loess; SL-L3 and SL-L4 loess at Ruma correlate with glacial cycles "D" and "E" loess, respectively, at Hungarian and Slovakian localities (table 1, figure 5). Our aminostratigraphy of loess units suggests that the double paleosol SL-S2 SS1 + SL-S2 SS1 at Ruma correlates with the BD1+BD2 paleosol complex in Hungary. Overall, these and other A/I ratios measured in samples from Ruma suggest late- and middle-Pleistocene ages for Ruma's loess-paleosol sequence, which can be correlated with aminostratigraphic units in Hungary, Slovak and Czech sites (Oches & McCoy, 1995a, 1995b).

Figure 5 Aminostratigraphy of the Ruma section compared with Hungarian (H), Slovakian (SK), Austrian (A), Czech (CZ) and German (D) localities for glacial cycles B, C, D, and E, corresponding to marine oxygen-isotope stages 2-5, 6-7, 8-9 and 10-11 for the genus Trichia and Pupilla. Pointed lined shows present day air temperatures of investigated sites (Marković et al., in press).

AAR geochronology results from the Ruma sections confirms the interpretation of the previous chronostratigraphic scheme of Marković (2000). According to our present chronostratigraphic model, loess-paleosol sequences SL L1 LL1, SL L1 SS1, SL LL2 and SL S1 formed during glacial cycle B (Kukla, 1975), corresponding with marine oxygen-isotope stages (MIS) 2, 3, 4 and 5. Horizons SL L2 loess and SL S2, which is a complex of two strong paleosols, correspond with glacial cycle C and MIS 6 and 7. The next loess and strong

36Milutin Milankovitch Anniversary Symposium Field Guide Book

developed interglacial paleosol, SL L3 and SL S3 formed during glacial cycle D of MIS 8 and 9. The basal loess, L4, accumulated during the later part of cycle E, correlated with MIS 10. Following this chronology, a significant correlation is observed between the clay content and magnetic susceptibility variations of the Ruma loess-palesol sequence and the SPECMAP (Imbrie et al., 1984) delta-^{18O variations (figure 6).}

5. PALEOCLIMATIC AND PALEOENVIRONMENTAL INTERPRETATION

The position of the Ruma section, in the shadow of Fruška Gora mountain range, is a setting that was susceptible to relatively low dust accumulation and dry paleoclimatic conditions. Present mean annual rainfall is less approximately 15% less along southern slopes than the average precipitation along the northern side of the range.

Magnetic susceptibility data and clay content variations of Ruma's loess-paleosol sequences demonstrate fluctuations from humid to drier paleoclimatic conditions during the last ca. 350,000 years (figure 6). This paleoclimatic trend is supported by the succession of paleosols from forest to dry steppe soils. The oldest strongly developed forest soil, SL S3, with a clay content ranging from 31 to 46% indicates warm and humid paleoclimatic conditions. Paleosol SL S2 SS2 is a transitional steppe-forest soil with clay content of 29-33%. Weakly developed fossil chernozem SL S2 SS1 has 23% clay. In the absence of paleodepressions, SL S1 has 25% clay, and the clay fraction of SL L1 SS1 is only 19%. Maximum carbonate content is 33% in SL L4 loess, in contrast to very low values of carbonate in paleosols.

Figure 6 Correlation between the magmetic susceptibility and clay record of the Ruma loess-palesol sequence and SPECMAP delta-18O series (Marković et al., in press).

A sharp contrast between high values of magnetic susceptibility measured in paleosols and low values from loess units measured at Ruma profile reflects magnetic enchancent via pedogenesis and is similar to that in Chinese and Central Asian loess deposits (e.g. Maher and Thompson, 1999). Magnetic susceptibilty record of Ruma loess-paleosol sequences provides similarity with magnetic measurements at Paks, Hunary (Sartori, 1999) Mostistea, Romania

5. PALEOCLIMATIC AND PALEOENVIRONMENTAL INTERPRETATION

The position of the Ruma section, in the shadow of Fruška Gora mountain range, is a setting that was susceptible to relatively low dust accumulation and dry paleoclimatic conditions. Present mean annual rainfall is less approximately 15% less along southern slopes than the average precipitation along the northern side of the range.

Magnetic susceptibility data and clay content variations of Ruma's loess-paleosol sequences demonstrate fluctuations from humid to drier paleoclimatic conditions during the last ca. 350,000 years (figure 6). This paleoclimatic trend is supported by the succession of paleosols from forest to dry steppe soils. The oldest strongly developed forest soil, SL S3, with a clay content ranging from 31 to 46% indicates warm and humid paleoclimatic conditions. Paleosol SL S2 SS2 is a transitional steppe-forest soil with clay content of 29-33%. Weakly developed fossil chernozem SL S2 SS1 has 23% clay. In the absence of paleodepressions, SL S1 has 25% clay, and the clay fraction of SL L1 SS1 is only 19%. Maximum carbonate content is 33% in SL L4 loess, in contrast to very low values of carbonate in paleosols.

Figure 6 Correlation between the magmetic susceptibility and clay record of the Ruma loess-palesol sequence and SPECMAP delta-18O series (Marković et al., in press).

A sharp contrast between high values of magnetic susceptibility measured in paleosols and low values from loess units measured at Ruma profile reflects magnetic enchancent via pedogenesis and is similar to that in Chinese and Central Asian loess deposits (e.g. Maher and Thompson, 1999). Magnetic susceptibilty record of Ruma loess-paleosol sequences provides similarity with magnetic measurements at Paks, Hunary (Sartori, 1999) Mostistea, Romania

37Milutin Milankovitch Anniversary Symposium Field Guide Book

(Panaiotu et al., 2001) and Koriten, Bulgaria (Jordanova and Petersen, 1999). MS correlation between Ruma loess-paleosol sequences and other central and southeastern European sites support chronostratigraphic subdivision based on AAR measurements.

The discovery of bones from 8 bear skeletons in SL L3 loess is of special interest. All the bones were found within a limited area of only 500 m^{2 (fig. 7). According to the character of the teeth, it is apparent that the skeletons belong to old individuals. The dimensions of the small skeletons indicate the presence of middle Pleistocene species Ursus deningeri (Rabeder and Withalm, personal communication). It is possible that the bears began migration as climate cooled following the warm and humid period associated with SL S3 soil formation. It is possible that old and sick individuals could not endure the migration and died in burrows formed within the loess.}

Fossil gastropod fauna from the loess and paleosols at Ruma provide additional important paleoenvironmental information. During the middle Pleistocene, the dominant snail assemblage in loess units SL L4, SL L3 and SL L2 is equivalent to the Chondrula tridens fauna of Ložek (1964, 2001), with the dominant species Chondrula tridens, Helicopsis striata, Pupilla triplicata, Vallonia costata, Truncatellina cylindrica and Coclicopa lubricella. This loess snail faunal type indicates the existence of dry steppe environmental conditions with dry and relatively cool paleoclimate. The presence of Granaria frumentum in a few levels suggests occasional brief episodes of warmth. In contrast the presence of Pupilla sterri and an abrupt decrease in total number of individuals in the lower part of SL L2 loess indicates the onset of much colder conditions.

The Upper Pleistocene snail assemblage suggests drier environmental conditions than in older loess and paleosol units. The interglacial species Helix pomatia was found in the middle part of SL S1 paleosol. An equivalent of Ložek’s (1964, 2001) Helicopsis striata fauna is identified in the upper part of SL S1 and SL L1 SS1 paleosols and SL L1 LL1 and SL L1 LL2 loess units. Overall, the snail assemblage of the last glacial cycle loess and paleosols is qualitatively and quantitatively very poor. During excavation of raw materials in 1978, workers found fragments of a wooly mammoth skeleton (Mammuthus primigenius; Milić, 1978) at the base of SL L1 LL 2 loess, adding to the paleoecological picture of Ruma's upper Pleistocene "warm" loess environment.

Hydrolysis index values, following Thorez (1985), suggest a warm and humid paleoclimatic period during the formation of paleosols SL S3 and SL S2 SS2. A gradual decrease in weathering can be followed from SL S2 SS1 through SL S1 and SL L1 SS1 soil and loess sequences. The orthoclase / (orthoclase + quartz) and illite / (illite + quartz) ratios in the Ruma loess sequence support the climatic changes inferred from the hydrolysis index. Both illite and orthoclase are sensitive to hydrolysis by rainwater, whereas quartz is much more stable in a temperate climate, so larger values for both ratios indicate stronger weathering. The hydrolysis index curve for the Ruma sequence correlates well with both orthoclase / (orthoclase + quartz) and illite / (illite + quartz) ratios. The changes in the hydrolysis index of Thorez (1985) and in the orthoclase / (orthoclase + quartz) and illite / (illite + quartz) ratios indicate a steady overall decreases in weathering rates after formation of the SLS3 and SLS2 SS2 paleosols, which also suggests a progressive decrease in precipitation during the later parts of the Quaternary, perhaps with some overall cooling and precipitation decrease.

Fossil gastropod fauna from the loess and paleosols at Ruma provide additional important paleoenvironmental information. During the middle Pleistocene, the dominant snail assemblage in loess units SL L4, SL L3 and SL L2 is equivalent to the Chondrula tridens fauna of Ložek (1964, 2001), with the dominant species Chondrula tridens, Helicopsis striata, Pupilla triplicata, Vallonia costata, Truncatellina cylindrica and Coclicopa lubricella. This loess snail faunal type indicates the existence of dry steppe environmental conditions with dry and relatively cool paleoclimate. The presence of Granaria frumentum in a few levels suggests occasional brief episodes of warmth. In contrast the presence of Pupilla sterri and an abrupt decrease in total number of individuals in the lower part of SL L2 loess indicates the onset of much colder conditions.

The Upper Pleistocene snail assemblage suggests drier environmental conditions than in older loess and paleosol units. The interglacial species Helix pomatia was found in the middle part of SL S1 paleosol. An equivalent of Ložek’s (1964, 2001) Helicopsis striata fauna is identified in the upper part of SL S1 and SL L1 SS1 paleosols and SL L1 LL1 and SL L1 LL2 loess units. Overall, the snail assemblage of the last glacial cycle loess and paleosols is qualitatively and quantitatively very poor. During excavation of raw materials in 1978, workers found fragments of a wooly mammoth skeleton (Mammuthus primigenius; Milić, 1978) at the base of SL L1 LL 2 loess, adding to the paleoecological picture of Ruma's upper Pleistocene "warm" loess environment.

Hydrolysis index values, following Thorez (1985), suggest a warm and humid paleoclimatic period during the formation of paleosols SL S3 and SL S2 SS2. A gradual decrease in weathering can be followed from SL S2 SS1 through SL S1 and SL L1 SS1 soil and loess sequences. The orthoclase / (orthoclase + quartz) and illite / (illite + quartz) ratios in the Ruma loess sequence support the climatic changes inferred from the hydrolysis index. Both illite and orthoclase are sensitive to hydrolysis by rainwater, whereas quartz is much more stable in a temperate climate, so larger values for both ratios indicate stronger weathering. The hydrolysis index curve for the Ruma sequence correlates well with both orthoclase / (orthoclase + quartz) and illite / (illite + quartz) ratios. The changes in the hydrolysis index of Thorez (1985) and in the orthoclase / (orthoclase + quartz) and illite / (illite + quartz) ratios indicate a steady overall decreases in weathering rates after formation of the SLS3 and SLS2 SS2 paleosols, which also suggests a progressive decrease in precipitation during the later parts of the Quaternary, perhaps with some overall cooling and precipitation decrease.

38Milutin Milankovitch Anniversary Symposium Field Guide Book

Figure 7 Tree diagram of relation between depth and mineral ratios for Ruma loess-paleosol sequences (Marković et al., 2004).

Figure 8 Relation between profile depth and Illite/Q+Illite ratio values

(Marković et al., 2004).

A tree diagram of depth, mineral ratio indexes (illite to quartz and orthoclase to quartz ratios) and hydrolitic index was obtained by means of cluster analysis by using weighted pair-group averages and the Pearson correlation coefficient (figure 7). A significant correlation of these parameters for the Ruma paleosol sequence is observed. Illite to quartz plus illite mineral ratio reveals a positive correlation with soil depth (r = 0.694), while hydrolitic index also shows significant positive correlation with feldspar to quartz plus orthoclase ratio (r = 0.671) in the paleosols investigated (figures 8 and 9). Correlation fbetween these two groups remains positive, but with a low non-significant (r = 0.211) correlation coefficient.

39Milutin Milankovitch Anniversary Symposium Field Guide Book

Figure 9 Relation between hydrolitic index and Orthoclase /Q+Orthoclase

6. CONCLUSIONS

Investigations of Ruma's loess-paleosol sequences during the last several years have established the importance of this site as a record of middle and late Pleistocene paleoclimate and paleoenvironment in Serbia. Especially interesting are thick pedogenetic layers formed in paleo-depressions, which were created during the last glacial cycle.

As the most extensively investigated Serbian exposure, this site enables the possibility of reconstructing local and regional environmental process and conditions during the middle and late-Pleistocene epoch. The first amino acid dating of loess-paleosol sequences in this region confirm stratigraphic and temporal correlations with other central and southeast European sites. Sedimentological, pedological, magnetic and paleontological evidence all suggest periods of drier environmental conditions in this region than in other parts of the Pannonian (Carpathian) basin during the last ca. 350,000 years.

7. REFERENCES

40Milutin Milankovitch Anniversary Symposium Field Guide Book

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