The Danube terrace staircases in Hungary developed between the uplifting areas of the Transdanubian Range and the North Hungarian Mountains and the subsiding Little Plain and Great Hungarian Plain. Different uplift and subside rates and periodic climate changes affected the formation of the terraces during the Late Pliocene and Pleistocene. The chronology and correlation of the Danube terrace system in Hungary are based on the geomorphic position of the terrace segments, rare palaeontological findings (e.g. Pécsi, 1959; Kretzoi and Pécsi, 1982; Virág and Gasparik, 2012), U/Th ages (e.g. Kele 2009; Sierralta
Sedimentological and petrological data also support the correlation of the terraces, e.g. roundness of gravels (Pécsiné Donáth 1958; Burján 2000) and heavy minerals (Burján 2003). In the NE part of the Transdanubian Range, at the Gerecse Hills, a new terrace system was established by Csillag
The study area is the Pest Plain (Figs. 1 and 2). It is situated near River Danube in the surroundings of Budapest, between hilly areas (Gödöllő Hills, Buda Mountains and Visegrád Mountains). The basement of this plain lies about 600–1500 m in depth, and consists of Upper Triassic and Lower Jurassic dolomite and limestone, which was formed from the sediments of the Tethys sea (Haas
On the uplifting areas northwest from the Pest Plain, six or maximum eight terraces were developed at the Danube band, according to Pécsi (1959) and Kretzoi & Pécsi (1982), and in the Gerecse Hills, eleven terraces were recently identified by Csillag
The valley of the Danube is located at about 122 m asl. in the northern part of the Pest Plain and at 97 m asl. in the southern part of it, at Budapest. Towards south, the terraces lie gradually at lower altitude in the direction of the sinking Great Hungarian Plain, where the river built a huge alluvial fan.
First of all, the position and characteristics of the terraces on the Pest Plain were studied in detail by Pécsi (1958, 1959, 1996). According to him, terraces V and IV occur only in the south-eastern part of the Pest Plain. Terrace V is built up from gravel with about 14 m thickness, while terrace IV consists of a 1–2 m thick gravel layer with 3–4 m sand on it. The sediments show signs of cryoturbation and solifluction. The gravels are mainly from quartz and quartzite, and partly from andesite of the Visegrád Mountains, and limestone from the Gerecse Hills of the Transdanubian Range. In some places, these sediments are covered by travertine. Based on fossils of
Terrace III runs in a narrow range between the older and younger terraces, 27–30 m above the recent level of the Danube. Its age is Riss (Saale, MIS 8 – MIS 6) according to Pécsi (1959), or minimum 170 ka (Ruszkiczay-Rüdiger
Terrace II also consists of two levels. Terrace IIb can be followed through the Pest Plain parallel to the Danube. The gravel layer of this terrace is about 7–10 m thick and lies at about 15–20 m above the current level of the Danube. The quartz and quartzite gravels of the younger terrace sediments are more rounded (Pécsiné Donáth 1958).
Terrace IIa is 8–10 m above the current level of the Danube and developed at the end of the Pleistocene, during the Late Würm (Late Weichselian) period. The stair of this terrace started to form after the Last Glacial Maximum, or about 19–17 ka ago (Gábris, 2006, 2013). Usually, this terrace is covered by aeolian sand. 18±2.5 ka old fluvial sediments and 16–0.6 ka old aeolian sands with paleosoils between them were dated by luminescence (TL, IRSL) and radiocarbon methods at Kisoroszi and Dunavarsány (Fig. 2, Ujházi
Terrace I is represented by overbank sediments at 5–7 m above the current level of the Danube. It is built up of fluvial sand and silt, which were deposited during the Early Holocene. The lowest level along the river also consists of overbank deposits, but in the lower position, 0–5 m above the level of Danube (Pécsi, 1996). In the abandoned arms of the Danube swampy environments developed.
The terrace levels are not in their original position because the neotectonic movements replaced them into gradually lower positions in the direction of the sinking Great Hungarian Plain (Fig. 3).
The surface of the terraces was altered during the forthcoming interglacial and glacial periods. They were covered mainly by aeolian sediments (loess or aeolian sand), and in some places by fluvial sediments and travertine. Under the modern soil layer mostly Weichselian sediments can be found. During the cold and dry periods in the Weichselian open coniferous taiga forests and steppe mosaics were characteristic for the plain areas of Hungary (Járainé Komlódi, 2000). This climate and the scarce vegetation favoured the sand and silt movement by strong winds, first of all, during the Weichselian High Glacial in MIS 3, and the Last Glacial Maximum in MIS 2. Loess formation in MIS 3 and MIS 2 was documented in many places of Hungary (e.g. Sümegi and Krolopp, 1995; Novothny
For optically stimulated luminescence dating, the samples were collected by opaque PVC tubes from five outcrops on different terraces of the Danube (Table 1; Fig. 2). For environmental dose determination, about 1 kg bulk samples were collected from the near surroundings of each OSL samples. In addition, some sediment was taken into tight closed containers (plastic boxes) for water content measurements.
Location and main characteristics of the samples.
Location | Terrace level | Latitude (N) | Longitude (E) | Altitude (m asL) | Sample | Nr. | Depth (cm) | Sediment | Facies |
---|---|---|---|---|---|---|---|---|---|
Nagytarcsa gravel mine | V | 47.52822 | 19.25767 | 170.52 | Nt1 | 120.1. | 700 | medium sand with gravel | fluvial |
Mogyoród gravel mine | V | 47.58594 | 19.22269 | 247.66 | Mgy1 | 119.1. | 130 | fine sand | dune |
Csomád sand mine E wall | III | 47.67194 | 19.18694 | 146.49 | Csm1 | 122.1. | 160 | silty fine sand | dune |
Csomád sand mine W wall | III | 47.67131 | 19.18592 | 150.81 | Csm3 | 122.3. | 240 | fine-medium sand | fluvial |
Fót sand mine | III | 47.64511 | 19.17714 | 175 | Ft1 | 123.1. | 180 | fine-medium sand | slope, reworked fluvial |
Dk1 | 121.1. | 190 | medium sand | dune | |||||
Dk2 | 121.2. | 360 | medium sand | dune | |||||
Dunakeszi sand mine | IIb | 47.66083 | 19.15706 | 165.47 | Dk3 | 121.3. | 410 | medium sand | fluvial |
Dk4 | 121.4. | 590 | fine sand | fluvial | |||||
Dk5 | 121.5. | 740 | fine-medium sand | fluvial |
Two fluvial samples, medium-grained sand with gravel are from the Nagytarcsa gravel mine which represents terrace V according to the geomorphological map of Pécsi
Aeolian fine sand layers at 1.3 and 2.4 m depth were sampled from a dune on terrace V in the Mogyoród gravel mine (Fig. 4A). The ~3.5 m high dune is built up from fine and medium grained sand layers with cross stratification. Under the dune the gravel layer of the terrace is only 0.5–0.6 m thick, and contains mainly quartzite, weathered volcanic rock and subordinately gneiss gravels.
Four samples were collected for dating from the Csomád sand mine on terrace level III (Fig. 4F-H). Two aeolian silty fine sand samples are from the East wall of the mine at depth 1.6 and 3.2 m. The other two samples are fluvial fine-medium grained sands from the West wall of the mine from 2.4 and 4.4 m depth, which represent the sediments of a small stream. The sand bodies are cross-laminated and their thickness in the outcrops is about 2 and 3 m, respectively.
Reworked fluvial fine-medium sands of slope sediments were sampled for dating on terrace III in the Fót sand mine, from a depth of 1.8 and 3.5 m (Fig. 4C and D). The total thickness of these sediments is about 3 m and they show cross and planar lamination.
On terrace IIb, fluvial and aeolian fine and medium-grained sand samples were studied between depths of 1.9 and 7.4 m in the Dunakeszi sand mine (Fig. 4B). Here the minimum 2.5 m thick fluvial sand of a stream shows mainly planar bedding and contains thin gravel layers and lenses. Quartz, quartzite and relatively fresh volcanic rocks are frequent with a size of 0.3–1.0 cm. The thickness of the aeolian sand is about 2–3 m. It is cross-laminated and contains many rhizoconcretions.
Sample preparation for optically stimulated luminescence dating was carried out under subdued red light conditions. Quartz and K-feldspar grains were extracted from the 0.1–0.2 mm grain size fraction of the sediments using 20% H2O2 to remove the organic material, 10% HCl to dissolve carbonates, 0.01N Na2C2O4 for desaggregation and cleaning of the surface from the grains, and aqueous solution of sodium polytungstate (3Na2WO4 · 9WO3 · H2O, SPT) with 2.67 and 2.58 g/cm3 for density separation. After these treatments, the quartz separates were etched by 40% HF for 90 min, or samples Dk1-5 for 60 min, to eliminate the outer 10–15 μm layer from the surface of the grains which was affected by the environmental alpha radiation. Then, 10% HCl was used to dissolve fluorides which were precipitated during etching. Finally, the 0.10–0.16 mm quartz and feldspar grains were separated by dry sieving.
The grains were mounted in monolayer on stainless-steel discs using silicone oil spray. The size of the aliquots was 2 mm diameter (small aliquot) in the case of feldspar, and 5 mm diameter (medium aliquots) in the case of quartz due to the relatively weak OSL signal of the quartz of the studied samples.
Before gamma spectrometry measurements, the bulk samples were dried, and the >1 mm grains were crashed. The sediments were filled into Marinelli beakers and they were stored in the closed containers for more than 28 days to reach equilibrium between radon and its daughter isotopes.
Luminescence measurements were made by Risø TL/OSL DA- 15C/D and DA-20 readers in 2013 and 2019. Blue light stimulated luminescence of quartz was detected through a Hoya-340 filter, while infrared light stimulated luminescence of feldspar through a Schott BG-39 and Coring 7-59 filter combination. A calibrated 90Sr/90Y beta source was used for irradiation with a dose rate of about 0.092 Gy/s in 2013, and 0.081 Gy/s in 2019.
Single-Aliquot Regenerative-dose (SAR) OSL protocol (Wintley and Murray, 2006) was used on quartz, and post-IR IRSL (290 ºC) on feldspar (Thiel
K-feldspar was measured by post-IR IRSL290 protocol with 320°C preheat before IR stimulation at 50°C for 200 s, then at 290°C for 200 s, and illumination at 325°C for 100 s in the last step of each cycle according to Thiel
Residual doses and dose recovery ratios of the feldspar separates were measured after 12 h bleaching on changeable (sometimes cloudy) sunlight in winter except for the saturated samples. The bleachability of the post-IR IRSL290 signal of four feldspar separates was also observed by bleaching them on bright sunlight in summer (in August) for 4, 8, 12, 16, 20, 26 and 30 h before the residual dose determination. The fading test according to Auclair
Calculation of the environmental dose rates is based on laboratory high-resolution gamma spectrometry measurements. They were made by Canberra GC3020 on 0.8–1.0 kg bulk samples, and provide U, Th and K concentrations. Dose rate conversion factors given by Adamiec and Aitken (1998), attenuation factors of Mejdahl (1979) were applied. 12.5±0.5% K concentration (Huntley and Baril, 1997) and 0.15±0.05 a-value (Balescu and Lamothe, 1994) were used during the calculation of the internal dose rate of feldspar. The cosmic dose rate was determined according to Prescott and Stephan (1982) and Prescott and Hutton (1994).
The water content of the sediments was determined at the time of sampling and after saturation by water in a laboratory. The results helped to estimate the water content of the dated sediments during the time period of burial. It was taken 5±1% for the dune sands, and 11±2%, 14±3% or 18±3% for the fluvial sediments (Table 2).
Dose rate determination.
Sample | Depth (cm) | U (ppm) | Th (ppm) | K (%) | Water content (dryw%) | Dose rate (Gy/ka) | |
---|---|---|---|---|---|---|---|
Quartz | K-feldspar | ||||||
Nt1 | 700 | 0.81 ± 0.02 | 2.49 ± 0.04 | 1.02 ± 0.01 | 18 ± 3 | 1.22 ± 0.09 | 1.85 ± 0.19 |
Nt2 | 790 | 0.75 ± 0.02 | 2.74 ± 0.03 | 1.04 ± 0.01 | 18 ± 3 | 1.23 ± 0.09 | 1.86 ± 0.19 |
Mgy1 | 130 | 1.72 ± 0.02 | 6.06 ± 0.05 | 0.79 ± 0.04 | 5 ± 1 | 1.69 ± 0.12 | 2.44 ± 0.17 |
Mgy2 | 240 | 2.00 ± 0.04 | 7.25 ± 0.06 | 0.83 ± 0.03 | 5 ± 1 | 1.85 ± 0.13 | 2.63 ± 0.19 |
Csm1 | 160 | 1.45 ± 0.02 | 4.15 ± 0.05 | 1.18 ± 0.04 | 5 ± 1 | 1.87 ± 0.13 | 2.57 ± 0.19 |
Csm2 | 320 | 2.17 ± 0.05 | 7.20 ± 0.06 | 1.12 ± 0.05 | 5 ± 1 | 2.14 ± 0.16 | 2.93 ± 0.21 |
Csm3 | 240 | 1.59 ± 0.02 | 5.01 ± 0.04 | 0.91 ± 0.04 | 14 ± 3 | 1.54 ± 0.11 | 2.25 ± 0.16 |
Csm4 | 440 | 1.53 ± 0.03 | 4.82 ± 0.04 | 0.90 ± 0.03 | 14 ± 3 | 1.48 ± 0.10 | 2.18 ± 0.15 |
Ft1 | 180 | 1.95 ± 0.05 | 3.81 ± 0.04 | 0.80 ± 0.02 | 11 ± 2 | 1.50 ± 0.10 | 2.22 ± 0.15 |
Ft2 | 350 | 1.95 ± 0.06 | 3.17 ± 0.03 | 0.83 ± 0.03 | 11 ± 2 | 1.46 ± 0.10 | 2.16 ± 0.15 |
Dk1 | 190 | 0.78 ± 0.01 | 1.95 ± 0.03 | 0.82 ± 0.03 | 5 ± 1 | 1.24 ± 0.09 | 1.86 ± 0.13 |
Dk2 | 360 | 1.22 ± 0.02 | 3.85 ± 0.04 | 0.81 ± 0.03 | 5 ± 1 | 1.42 ± 0.10 | 2.10 ± 0.15 |
Dk3 | 410 | 1.19 ± 0.03 | 3.10 ± 0.03 | 0.81 ± 0.03 | 11 ± 2 | 1.28 ± 0.09 | 1.93 ± 0.14 |
Dk4 | 590 | 1.42 ± 0.02 | 3.79 ± 0.04 | 0.89 ± 0.04 | 11 ± 2 | 1.41 ± 0.10 | 2.09 ± 0.15 |
Dk5 | 740 | 1.34 ± 0.03 | 4.18 ± 0.04 | 0.87 ± 0.04 | 11 ± 2 | 1.39 ± 0.10 | 2.07 ± 0.15 |
Sample preparation, luminescence, gamma spectrometry, and water content measurements were carried out at the Mining and Geological Survey of Hungary (MBFSZ, former Geological and Geophysical Institute of Hungary).
The results of dose rate determination are in Table 2. The optically stimulated luminescence test measurements indicated that quartz and K-feldspar fractions of the samples are good for precise age dating, except two samples with saturated quartz OSL and feldspar post-IR IRSL290 signals.
Dose recovery ratios of quartz are satisfactory, 1.05±0.02 on average (n=39, Table 3). Some aliquots were rejected due to an inadequate result of IR test (feldspar or mica contamination), or high recuperation, or bad recycling ratio. Recuperation of the accepted aliquots is low, 1.02±1.09 on average (n=403). Quartz OSL dating is based on equivalent doses of 23–56 aliquots per sample (Table 4). The De values of the studied quartz fractions have a relative error in a range of 3.9–9.6%, precision (reciprocal standard error) ~10–25, and relatively high dispersion. These characteristics were visualised in the bivariate plots (radial plots based on Galbraith, 1988; Galbraith and Roberts, 2012) of abanico plots (Dietze
Dose recovery ratios.
Sample | Dose recovery ratio | |
---|---|---|
Quartz OSL | K-feldspar post-IR IRSL290 | |
Mgy1 | 1.01 ± 0.10 | 1.02 ± 0.09 |
Mgy2 | 1.03 ± 0.02 | 1.00 ± 0.10 |
Csm1 | 0.98 ± 0.07 | 1.01 ± 0.08 |
Csm2 | 0.96 ± 0.09 | 1.02 ± 0.05 |
Csm3 | 0.99 ± 0.08 | 1.08 ± 0.05 |
Csm4 | 1.01 ± 0.06 | 1.10 ± 0.04 |
Ft1 | 0.99 ± 0.07 | 1.08 ± 0.01 |
Ft2 | 0.97 ± 0.05 | 1.02 ± 0.07 |
Dk1 | 0.99 ± 0.02 | 0.97 ± 0.11 |
Dk2 | 1.03 ± 0.04 | 0.97 ± 0.15 |
Dk3 | 0.98 ± 0.07 | 0.98 ± 0.13 |
Dk4 | 0.98 ± 0.05 | 0.99 ± 0.09 |
Dk5 | 1.02 ± 0.06 | 0.96 ± 0.14 |
In the case of sample Dk4 more than fifty aliquots were measured to get more symmetric distribution. Except for two samples, the overdispersion of the De-s changes between 12 and 22% (Table 4; Fig. 5A), indicating that the quartz of these sediments was probably well bleached at the time of deposition according to Olley (2004). Therefore, their age was calculated by the mean De values, which are almost identical to the central De-s, using the central age model of Galbraith
Dating result of quartz and K-feldspar
Quartz OSL | K-feldspar post-IR I2SL29O | K. -feldspar age/Quartz age | |||||||||||||||||
---|---|---|---|---|---|---|---|---|---|---|---|---|---|---|---|---|---|---|---|
Sample | Depth (cm) | n | De mean (Gy) | OD (%) | Age (ka) | n | De mean (Gy) | OD (%) | Residual dose (Gy) | Residual dose (%)** | Age (ka) | ||||||||
w. | s. | w. | s. | a. | no subtr. | w. subtr. | s. subtr. | no subtr. | w. subtr. | s. subtr. | |||||||||
Nt1 | 700 | 3 | 546* | >296 | |||||||||||||||
Nt2 | 790 | 3 | 537* | >289 | |||||||||||||||
Mgy1 | 130 | 24 | 62.9 ± 2.7 | 18 ±3 | 37.1 ±3.1 | 10 | 100.3 ±3.1 | 9± 2 | 14.6 ±0.6 | 14.6 | 9.5 | 41.0 ± 2.3 | 35.0± 2.1 | 1.10±0.11 | 0.94 ±0.10 | ||||
Mgy2 | 240 | 25 | 70.4 ± 3.7 | 22 ±3 | 38.1 ±3.3 | 9 | 99.7 ± 2.9 | 7 ± 2 | 19.2 ±3.0 | 7.4 ± 1.3 | 19.2 | 7.4 | 0.0 | 37.9 ± 1.9 | 30.6 ± 1.7 | 35.1 ± 1.8 | 0.99 ±0.10 | 0.80 ±0.08 | 0.92 ±0.09 |
Csm1 | 160 | 24 | 73.3 ±3.3 | 20 ±3 | 39.3 ±3.4 | 10 | 115.4 ±3.1 | 7 ± 2 | 18.7 ±4.1 | 7.4 ±0.5 | 16.2 | 6.4 | 12.6 | 44.9 ± 2.3 | 37.7 ± 2.0 | 42.0 ± 2.2 | 1.14±0.11 | 0.96 ±0.10 | 1.07 ±0.11 |
Csm2 | 320 | 23 | 91.0 ±3.6 | 18 ±3 | 42.6 ±3.6 | 11 | 126.2 ±4.8 | 11±3 | 16.3 ±3.9 | 13.0 | 1.0 | 43.1 ± 2.4 | 37.5 ± 2.2 | 1.01 ±0.10 | 0.88 ±0.09 | ||||
Csm3 | 240 | 25 | 43.9 ± 2.9 | 29 ±4 | 28.5 ± 2.8 | 9 | 69.6 ± 1.7 | 6± 2 | 13.4±3.6 | 19.2 | 7.9 | 30.9 ± 1.8 | 25.0 ± 1.5 | 1.09 ±0.12 | 0.88 ±0.10 | ||||
Csm4 | 440 | 24 | 45.7 ± 2.3 | 21±3 | 30.9 ± 2.6 | 11 | 76.5 ± 2.2 | 8± 2 | 13.3 ± 2.5 | 17.4 | 12.0 | 35.2 ± 2.1 | 29.0 ± 1.8 | 1.14 ±0.12 | 0.94 ±0.10 | ||||
Ft1 | 180 | 27 | 22.8 ±0.9 | 18 ±3 | 15.1 ± 1.2 | 11 | 35.0 ±0.9 | 7 ± 2 | 7.8 ±0.2 | 3.6 ±0.4 | 22.2 | 10.2 | 4.3 | 15.8 ±0.9 | 12.3 ±0.7 | 14.2 ±0.8 | 1.05 ±0.10 | 0.81 ±0.08 | 0.94 ±0.09 |
Ft2 | 350 | 25 | 33.3 ±0.9 | 12 ± 2 | 22.8 ± 1.8 | 11 | 52.5 ± 1.5 | 9± 2 | 11.5 ±3.5 | 21.9 | 6.3 | 24.3 ± 1.4 | 19.0 ± 1.2 | 1.07 ±0.10 | 0.83 ±0.08 | ||||
Dk1 | 190 | 24 | 16.8 ±0.7 | 21±3 | 13.6 ± 1.2 | 12 | 33.2 ±0.6 | 5± 1 | 7.4 ± 1.0 | 22.3 | 23.9 | 17.9 ± 1.1 | 13.9 ±0.9 | 1.31 ±0.14 | 1.02 ±0.11 | ||||
Dk2 | 360 | 25 | 20.0 ± 1.0 | 22±4 | 14.1 ± 1.2 | 11 | 35.7 ±0.5 | 4± 1 | 10.0 ±0.9 | 3.9 ±0.2 | 28.1 | 10.8 | 17.1 | 17.0 ±0.9 | 12.2 ±0.7 | 15.2 ±0.8 | 1.21 ±0.12 | 0.87 ±0.09 | 1.08 ±0.11 |
Dk3 | 410 | 26 | 19.4 ± 1.2 | 30±4 | 15.2 ± 1.5 | 11 | 35.7 ±0.9 | 7 ± 2 | 9.2 ±0.2 | 25.9 | 17.7 | 18.5 ± 1.1 | 13.7 ±0.9 | 1.22 ±0.14 | 0.90 ±0.10 | ||||
Dk4 | 590 | 56 | 21.2 ±0.7 | 22 ± 2 | 15.0 ± 1.2 | 12 | 39.3 ± 1.0 | 7 ± 2 | 9.0 ± 2.2 | 22.9 | 19.9 | 18.8 ± 1.1 | 14.5 ±0.9 | 1.25 ±0.13 | 0.96 ±0.10 | ||||
Dk5 | 740 | 29 | 21.9 ±0.8 | 17 ±3 | 15.8 ± 1.3 | 10 | 39.8 ±0.7 | 4± 1 | 10.6 ±0.3 | 26.7 | 17.8 | 19.2 ± 1.1 | 14.1 ±0.8 | 1.22 ±0.12 | 0.89 ±0.09 |
n: number of aliquots; OD: overdispersion; *: 2xD0; **: residual dose in % of the measured natural dose;
w: residual dose after 12 h exposure to changeable sunshine in winter;
s: residual dose after 4 h exposure to bright sunlight in summer;
no subtr.: feldspar age without subtraction of residual dose;
w. subtr.: feldspar age with subtraction of residual dose after 12 h exposure to changeable sunshine in winter;
s. subtr: feldspar age with subtraction of residual dose after 4 h exposure to bright sunlight in summer.
Figure 5 and overdispersion values in Table 4 show that the measured quartz medium aliquots have more heterogeneous dose distribution than in the case of K-feldspar small aliquots. As it can be supposed that the dated sediments were well bleached before burial, the more heterogeneous distribution of De-s in quartz is probably caused by the heterogeneity in the environmental beta dose rate. This can be the result of the microscopic fluctuations in the spatial distribution of feldspar containing beta emitter 40K (Mayya
Every measured aliquot of K-feldspar showed a good recycling ratio in the range of 1.0±0.1, and except three rejected aliquots they had recuperation under 5%. Residual doses after 12 h bleaching under changeable sunlight in winter are about 7–19 Gy on average (Table 4), while after the same duration of bleaching under bright sunshine in summer are about 3–5 Gy on average (which correspond to 13–28% and 4–10% of the mean natural equivalent doses respectively). The dose recovery ratios changed between 0.79 and 1.14 (from 0.96±0.14 to 1.1±0.04 on average, Table 3), but, the poor dose recovery ratio of post-IR IRSL290 signal of K-feldspar does not necessarily mean an inaccurate measurement of De (Buylaert
Two samples (Nt1 and Nt2) are saturated as their natural post-IR IRSL290 signals (Ln/Tn) lie above the saturation level. The minimum age of these samples was calculated with the 2*D0 values, which correspond to approximately 86% of the dose-response curve (Murray
In the bleaching experiment in natural sunlight during summer the measured post-IR IRSL290 residual doses of the four K-feldspar separates (Mgy2, Csm1, Ft1 and Dk2) ranged from 3.6±0.4 Gy to 7.4±0.5 Gy after 4 h exposure to bright sunshine, then they decreased more slowly with some scatter, and they were between 3.0±0.1 Gy and 5.2±0.6 Gy after 12 h exposure to sunshine, then an unbleachable component ranged from 2.5±0.7 Gy to 5.2±0.3 Gy after 30 h exposure to bright sunshine. The latter corresponds to 3–8% of the measured K-feldspar post-IR IRSL290 natural doses. K-feldspar of samples Mgy2 and Csm1 bleached slightly more rapidly than that of samples Dk2 and Ft1 (Fig. 6). Residual doses measured after 12 h exposure to changeable sunshine in winter varied from 7.4±1.0 Gy to 19.2±3.0 Gy and correspond to about 13–28% of the measured K-feldspar post-IR IRSL290 natural doses.
Except for one sample (Mgy2), the feldspar ages without residual dose subtraction are older than the quartz ages of the same samples, and the ratio of them range between 1.01±0.10 and 1.31±0.14 (Table 4). But, taking into account the 1 sigma error the two sets of ages agree in the case of samples Mgy1–2, Csm1–4 and Ft1–2, while the K-feldspar ages of samples Dk1–5 agree within 2 sigma error limit with quartz ages.
Using the same post-IR IRSL290 protocol on coarse-grain feldspar, there are some published data of residual doses, e.g. Alexanderson and Murray (2012) measured about 12 Gy residual dose in glaciofluvial sediments after 5 h bleaching in solar simulator in samples with 20–55 Gy natural dose; t6
Some experiments, e.g. Buylaert
Our bleaching experiment in bright sunlight in summer gave similar results (between 2.5±0.7 and 5.2±0.3 Gy residual doses after 30 h bleaching) to most of the above mentioned earlier studies, among them, the outcomes of residual measurements of Thiel
In the southern part of the study area at Nagytarcsa, the fluvial gravelly sand layers of Danube terrace V, which contain saturated quartz and feldspar, are older than ~ 296 ka according to feldspar post-IR IRSL290 minimum age based on 2*D0 values. Therefore, they were formed earlier than the MIS 7 period. This minimum age is not in conflict with the traditional terrace chronology of Pécsi (1959), Kretzoi and Pécsi (1982), and the 800 ka minimum age (Ruszkiczay-Rüdiger
In the central part of the Pest Plain, the two aeolian fine sand layers on terrace V in the Mogyoród gravel mine are about 37–38 (±3) ka old based on quartz ages (Table 4). In the case of the lower sample, the K-feldspar post-IR IRSL290 age without the subtraction of any residual dose and the quartz OSL age are in excellent agreement and their ratio is 0.99±0.10. Consequently, after residual dose subtraction, the ratio between feldspar and quartz ages are 0.80±0.08 and 0.92±0.09, depending on the bleaching conditions. In the upper sample, the age of feldspar without residual subtraction is older than the quartz age, while after the subtraction of the winter residual dose, it is younger than the quartz, the ratio of the feldspar age to quartz age is 1.10±0.11 and 0.94±0.10, respectively (Table 4).
Here, the ages of the dune sand samples indicate wind activity in the cold and dry period of MIS 3 on the surface of terrace V. Aeolian sediments with similar ages were identified in other parts of Hungary, e.g. the ~39 ka old wind-blown sand in the southern part of Hungary at Katymár (Sümegi
In the northern part of the study area, on terrace III, the dated two aeolian silty fine sand samples in the East wall of the Csomád sand mine, deposited 43±4 and 39±3 ka ago in MIS 3, according to the quartz OSL ages. The post-IR IRSL290 age of feldspar without residual-subtraction is similar to the age of quartz in the lower sample. In the case of the upper sample, the quartz age is between the age of feldspar without residual subtraction or with the subtraction of the summer residual dose after 4 h exposure to bright sunlight and the feldspar age after the subtraction of the winter residual dose. The last one is the closest to the quartz age, their ratio is 0.96±0.10 (Table 4).
The ages of the quartz in the fluvial sand samples in the West wall of this mine are 31±3 and 29±3 ka. The feldspar without residual subtraction gives older ages than the quartz with ratio 1.14±0.12 (Csm4) and 1.09±0.12 (Csm3). Meanwhile, after winter residual dose subtraction, the feldspar ages are younger, they are 0.94±0.10 (Csm4) and 0.88±0.10 (Csm3) of the quartz ages.
The ages of the dated samples in this mine indicate the formation of a sand dune in MIS 3, and fluvial sedimentation of a small stream about the transition from MIS 3 to MIS 2 on the surface of terrace III, which was formed minimum 170 ka ago (Ruszkiczay-Rüdiger
In the Fót sand mine, also on the area of terrace III, the dated lower and upper sand layers of the slope sediments with reworked fluvial material, deposited during the MIS 2 period, 23±2 and 15±1 ka ago, based on quartz dating. The relation between the feldspar and quartz ages shows similar tendencies to most of the other dated samples. The feldspar ages without residual subtraction are older than the quartz ages with ratios 1.07±0.10 and 1.05±0.10, while they are younger than the quartz after winter or summer residual subtraction, with ratios 0.83±0.08, 0.81±0.08 and 0.94±0.09. The lower slope sediment was probably deposited during cold period, in the Last Glacial Maximum, because loess layers with similar ages were dated to the same periods at Katymár (~22.5 ka BP, Sümegi
On terrace IIb, in the Dunakeszi sand mine, fluvial sand layers of a stream were deposited about 15–16(±1) ka ago, and the age of the sand layers in a dune is about 14±1 ka, according to quartz dating. Here is the largest difference between the feldspar ages which were calculated without residual dose subtraction and the quartz ages, the ratio of them ranges from 1.21±0.12 to 1.31±0.14 (Table 4). The feldspar ages after winter residual dose subtraction are younger than the quartz ages (feldspar age/quartz age is 0.87±0.09 – 0.96±0.10) except for the uppermost sample. Meanwhile, the feldspar of sample Dk2 after the subtraction of the summer residual dose gives an older age than the quartz does. The ages of the dated stream sediments and dune sands prove fluvial, and then aeolian activity during MIS 2 on the surface of terrace IIb, which developed a minimum 100 ka ago. In the southern part of the study area, fluvial sand with a similar age (~16 ka) was dated by TL method at Dunavarsány (Fig. 2; Ujházi
The 15-16(±1) ka old stream sediments of the Dunakeszi sand mine probably were deposited during the Oldest Dryas and the Allerød-Bølling interstadial, while the formation of the 14±1 ka old dune corresponds to the colder and drier period of the Allerød-Bølling according to the climate reconstruction of Kiss
Taking into account the differences between the ages of the dated two minerals, to get the same feldspar ages as the quartz ages, the assumable residual doses of the feldspar are set to be between 0 and 15±1 Gy (Csm1) or 0 and 24±2% (Dk1) of the measured natural doses (Table 4). These results imply that in most cases it is necessary to subtract some residual dose from the measured natural dose of feldspar before age calculation.
Optically stimulated luminescence dating of sandy fluvial, aeolian and slope sediments, collected on the Danube terraces of the Pest Plain serves new ages for this area where the numerical age data and the palaeontological findings are very scarce. Moreover it gives an opportunity for the comparison of coarse-grain quartz OSL and K-feldspar post-IR IRSL290 ages of the same sediments.
The measured quartz medium aliquots show more heterogeneous dose distribution than the K-feldspar small aliquots. Probably, this is caused by the heterogeneity in the environmental beta dose rate and the internal alpha dose rate.
The feldspar post-IR IRSL290 ages without residual dose subtraction are older than the quartz OSL ages, except for one sample, which quartz and feldspar ages are almost identical. But, the two sets of ages are overlapping within 1 or 2 sigma error.
Our bleaching experiment showed that the residual dose of feldspar is from 2.5±0.7 Gy to 5.2±0.3 Gy or 3–8% of the measured natural dose after 30 h exposure to bright sunshine. Based on comparison with the quartz ages the assumable residual doses range from 0 Gy to 15±1 Gy and amount to 24±2% of the measured natural doses. Therefore, in most cases of our samples, some residual dose subtraction is necessary before the calculation of the post-IR IRSL290 ages. However, without quartz OSL age data, or independent age control, the value of the residual dose of feldspar is uncertain. But, the range between the feldspar post-IR IRSL290 age without residual-subtraction, and the residual-subtracted age, can be considered as the maximum age range of the sediment. For subtraction, the residual dose after 4 h exposure to light in a solar simulator or bright sunshine is favourable, because the post-IR IRSL290 signal decreases rapidly in this time period.
The minimum age of the dated fluvial gravelly sand of terrace V is ~ 296 ka based on 2*D0 values of feldspar post-IR IRSL290. This age does not contradict the traditional terrace chronology and the earlier published age data of this terrace. The other studied sediments on the surface of the terraces V, III and IIb were deposited much later than the formation of the terraces. They indicate deposition of sediments in MIS 3 and MIS 2 periods: aeolian activity at 43–37(±3) ka and 14±1 ka ago, and fluvial sedimentation of small streams about 31–29(±3) ka and 16–15(±1) ka ago. The new ages help to reconstruct the surface developments of the Danube terraces. The age of the dated dune sands with coeval aeolian sediments in Hungary indicates the cold and dry periods with strong wind activity of the Late Weichselian.