1. bookAHEAD OF PRINT
Journal Details
License
Format
Journal
First Published
04 Jul 2007
Publication timeframe
1 time per year
Languages
English
access type Open Access

Post-IR IRSL chronology of paleo-lacustrine sediments from yardangs in the Qaidam Basin, ne Tibetan Plateau

Published Online: 13 Mar 2021
Page range: -
Received: 15 Feb 2019
Accepted: 15 Apr 2020
Journal Details
License
Format
Journal
First Published
04 Jul 2007
Publication timeframe
1 time per year
Languages
English
Abstract

The Qaidam Basin preserves the largest Yardang field on Earth, and yardangs are intriguing landforms for studies of the paleo-environment and aeolian processes. Formation of yardangs involved both the initial lacustrine deposition and the subsequent wind-erosion processes. However, the timings of both processes in the Qaidam Basin are still controversial due to limited age data and unsuitable dating methodology. In this paper, we first compared two optical dating methods to determine the suitable one for the study area, then investigated the geomorphic processes based on the new ages. Two-step post-IR IRSL (pIRIR) and multi-elevated-temperature pIRIR (MET-pIRIR) methods of feldspar, were applied to date lacustrine sediments on the top parts of yardangs to decipher the transition time from depositional to an erosional environment. Comparisons of the two methods demonstrated that the influence from anomalous fading was very minimal thus negligible for MET-pIRIR method, as proved by the De plateau between MET-pIRIR250 and MET-pIRIR290; while the pIR50IR250 signals suffered from fading obviously, which was difficult to be corrected due to the high De close to saturation. Consequently, the chronology in this study was based on the MET-pIRIR250 method, potentially offering reliable ages of over 200 ka. Seven MET-pIRIR250 ages of 201–336 ka suggested that a mega-Qaidam Lake (>2714 m a.s.l. on Google Earth) maintained until Marine Isotopic Stage (MIS) 7. The absence of sediments since ca. 200 ka implied wind-erosion and yardang formation since MIS6. This transition from lacustrine to a wind-erosion environment was interpreted as a response to the glacial-interglacial scale climatic changes.

Keywords

Introduction

Yardang is a typical wind-erosional landform in the arid and hyper-arid areas on the Earth (Goudie, 2007; Al-Dousari et al., 2009), and is a common landform on the Mars as well (Xiao et al., 2017, Anglés and Li, 2017; Wang et al., 2018). Studies on the evolution of Yardang have made significant progress attributed to the development of methods, e.g. remote sensing and geographic information system (Goudie, 2007), exposure dating (Wu et al., 2019) and erosion rate testing (Rohrmann et al., 2013) of 10Be.

The yardang field in the Qaidam Basin (QB), with an area of 3.88 × 104 km2, is the largest one on the Earth (Halimov and Fezer, 1989), and its extreme environments (high, cold, windy, arid and low pressure) make it an ideal terrestrial analogue site for aeolian geomorphologic studies on the Mars (Xiao et al., 2017, Anglés and Li, 2017; Wang et al., 2018). These yardangs indicate a transition from lacustrine to wind-eroded condition (Kapp et al., 2011; Rohrmann et al., 2013). The materials eroded from the yardangs can be redeposited into the downwind dune fields and loess in the eastern and southern QB (Yu and Lai, 2012, 2014; Yu et al., 2013, 2015a, 2015b) and also in the Chinese Loess Plateau (CLP) (Bowler et al., 1987; Kapp et al., 2011; Pullen et al., 2011; Rohrmann et al., 2013; Lai et al., 2014; Mischke et al., 2015). However, the time of the transition from lacustrine and wind-erosion environmental, i.e., the formation of yardangs, is still controversial. Earlier studies based on 14C dating proposed a mega-Qaidam Lake during Marine Isotopic Stage (MIS) 3 (Chen and Bower, 1986; Zhang et al., 2008), while the paleo-lacustrine sediments were dated to MIS5 by quartz Optically Stimulated Luminescence (OSL) dating (Lai et al., 2014). Depending on the regional geomorphological evolution, the formation time of the yardangs (onset of wind-erosion) is closely related to the above issues, but still unclear.

OSL dating has been applied in the QB to date both fluvial/lacustrine and aeolian sediments (e.g., Sun et al., 2010; Yu and Lai, 2012, 2014; Yu et al., 2013, 2015b, 2016; Lai et al., 2014). The quartz OSL signals, however, have been shown to saturate at relatively low doses of ~150 Gy on the CLP (Buylaert et al., 2008; Chapot et al., 2012), making it difficult to date the old (Pleistocene) lacustrine sediments in yardangs. Alternatively, the post-IR IRSL (pIRIR) dating of feldspars (Thomsen et al., 2008), with a much higher saturate dose up to ~1000 Gy (Li et al., 2018), has the potential advantages. Two-step pIRIR procedure (Thomsen et al., 2008; Buylaert et al., 2009) and multiple-elevated-temperature (MET) pIRIR procedure (Li and Li, 2011) have been proposed for feldspar pIRIR dating. Compared with the two-step pIRIR signals, the MET-pIRIR signals are less affected by fading but more difficult to be sufficiently bleached (Li and Li, 2012). However, no studies have shown which method is more suitable for such old sediments on the Tibetan Plateau (TP). In this study, both methods were applied to determine a proper dating method for the lacustrine sediments from yardangs in the central QB, and to offer reliable chronology for the transition from lacustrine to wind-erosional environment and geomorphic evolution (yardang formation).

Yardangs and samples

QB is a tectonically controlled depression on the northeastern TP and surrounded by Mountains (Fig. 1). Nowadays, with a potential-evaporation/precipitation ratio of > 100 (Chen and Bowler, 1985, 1986; Bowler et al., 1986), the extreme arid QB is dominated by playas/salt lakes and aeolian landforms. Modern meteorological data of 1971–2010 showed that the gale (wind speed ≥17m/s) days reached 163 d/yr (Zhang et al., 2014). Consequently, the wind erosion prevails and now yardangs cover ca. 1/3 area of the QB (Kapp et al., 2011), with the estimated erosion rate as ~0.125–0.29 mm/yr (Kapp et al., 2011; Rohrmann et al., 2013) during the Quaternary. Yardang orientations change from NNW-SSE in the northwestern part to WNW-ESE in the southeastern part corresponding to the changes of wind direction (Li et al., 2016; Hu et al., 2017).

Fig. 1

Landform (A-B) and sampled yardangs (C-D) in the Qaidam Basin. The elevations measured by differential GPS were used in Fig. 1C as it's more accurate.

Some road-cut sections display the stratigraphy of yardangs (Fig. 2), with heights of ~5–15 m, in the north of Qarhan Salt Lake (QSL) region. All these sections show horizontal or sub-horizontal strata with greenish, reddish and brownish layers, indicating typical lacustrine characteristics. The horizontal beddings demonstrate the limited influences from tectonic activities, i.e., not too old, which was an important criterion for us to identify the relatively young stratigraphy in the field. To reveal the termination of lacustrine environment, OSL samples were mainly taken from the upper part of the higher yardangs, which might be less eroded. Seven OSL samples were collected from five sites (Fig. 1) with the top elevations of 2643–2671 m measured by differential GPS, which is ~50 m lower than that derived from Google Earth (2704–2721 m). Samples YD3-A, YD6-B and YD7-C are mainly composed of clay and silt, and YD6-A, YD7-B, YD8-B and YD9-B are mainly composed of silt and fine sand. The details of section lithofacies and sampling locations are shown in Table 1.

Age results of MET-pIRIR250 with sample informations.

MET-pIRIR250
Sample Lithofacies and structuresYardang height (m)Grain size (μm)Depth (m)Altitude (m)Water content (%)Environmental Dose Rate (Gy·ka-1)De (Gy)Age (ka)
YD3-A Gray-brown clay, horizontal stratification34–111+10 a265615±55.4±0.61082±75201±25
YD6-A Gray-brown sandy clay, horizontal stratification5.563–905+10 a264415±54.8±0.3980±55203±20
YD6-B Gray-brown clay, horizontal stratification4–110.5+10 a264815±54.1±0.2985±74243±20
YD7-B Reddish-brown sandy clay, plane-parallel lamination6150–1804+10 a264015±52.8±0.1673±37240±16
YD7-C Clay-bank clay, horizontal stratification4–118+10 a263615±54.2±0.21061±75257±20.
YD8-B Yellow sand, plane-parallel lamination15150–18013+10 a265815±52.7±0.1902.2±92.2336±37
YD9-B Yellow sand, plane-parallel lamination8150–1808+10 a265915±52.6±0.1790.0±39.5306±20

aAn additional depth of 10 m was given to the samples in the calculation.

Materials and measurements

Samples were treated with HCl and H2O2 to remove carbonates and organic materials, respectively. The fraction of 4–11 μm (by settling samples using Stokes’ Law) or 150–180 μm (by wet sieving) were selected according to the grain composition of sediments. K-feldspars (KF) were extracted from the coarse grains (150–180 μm) by density separation (2.53–2.58 g/cm3) using sodium polytungstate and without HF etching. The KF were made into small aliquots with a diameter of 2 mm, and the 4–11 μm fractions were made into large aliquots.

Luminescence measurements were made by automated Risø TL/OSL readers (DA-20) with 90Sr/90Y beta sources in Linyi University and China University of Geo-science (Wuhan). The IRSL signals were detected through Schott BG39 and BG3 filters combination. A heating rate of 5°C/s in a nitrogen atmosphere was employed, followed by a pause of 10 s. The Lx and Tx were calculated using the initial 8 s signals of decay curves, with a subtraction of the last 100 s from 500 s for two-step pIRIR or the last 20 s from 100 s for MET-pIRIR. The dose rates and ages were calculated with the online Dose Rate Calculator (Durcan et al., 2015). The internal K contents of KF were estimated as 12.5±0.5% (Huntley and Baril, 1997). The a-value is 0.15±0.05 for coarse grain size (Balescu and Lamothe, 1994), and 0.086±0.038 for fine grain size (Rees-Jones, 1995). The measured water contents range only 0.31–5.47%, which are extremely low, especially for the paleo-lacustrine sediments. Combining their saturated water content of ~20–40% and the alternation of humid and arid environments during the past interglacial-glacial cycles, an average range of measured and saturate values, 15±5%, were estimated for these lacustrine sediments during their burial history. Taking the average wind erosion rate of 0.125 mm/yr (Rohrmann et al., 2013) into account, an additional depth of 10 m was added to the sample depths to calculate the ages. This estimation should be reasonable because the results increase slightly when the depth increases > 10 m. Five samples (YD6-B, YD7-C, YD7-B, YD8-B and YD9-B) are used for methodological studies illustrated as follow.

Methods and experiments
MET- pIRIR

In this study, the IR stimulations at 50, 100, 150, 200, 250, and 290°C with a preheat of 320°C were applied (Table 2a) after Li and Li (2011), using a single-aliquot regenerative-dose (SAR) protocol (Murray and Wintle, 2000; 2003), which is also for the two-step pIRIR.

Age results of MET-pIRIR250 with sample informations.

(a) MET-pIRIR250 of Feldspar(b) pIR50IR250 of Feldspar
StepTreatmentMeasuredTreatmentMeasured
1Dose-Dose-
2Preheat 320°C for 60 s-Preheat 280°C for 60 s-
3IRSL 50°C for 100 s-IRSL 50°C for 500 s-
4IRSL 100°C for 100 s-IRSL 250˚C for 500 sLx
5IRSL 150°C for 100 s-Test dose-
6IRSL 200°C for 100 s-Preheat 280°C for 60 s-
7IRSL 250°C for 100 sLxIRSL 50°C for 500 s-
8IRSL 290°C for 100 s-IRSL 250˚C for 500 sTx
9Test dose-Return to step 1
10Preheat 320°C for 60 s-
11IRSL 50°C for 100 s-
12IRSL 100°C for 100 s-
13IRSL 150°C for 100 s-
14IRSL 200°C for 100 s-
15IRSL 250°C for 100 sTx
16IRSL 290°C for 100 s-
17IRSL 320°C for 100 s-
18Return to step 1
Dose recovery test and luminescence properties

To examine the reliability of De estimation, dose recovery test was conducted on a well-bleached modern sand sample in the QSL region. For KF (150–180 μm), laboratory doses of 559 and 895 Gy were given to 3 and 5 aliquots (diameter of ~3 mm), respectively, followed by a measurement protocol in Table 2a. The ratios of measured to given dose for different MET-pIRIR signals were shown in Fig. 3A, which displays a plateau from 200°C to 290°C, with the best recovery ratio at 250°C.

Luminescence properties of MET-pIRIR signals were investigated (Fig. 4). Fig. 4A displayed a similar decay rate between fine-grain polymineral and coarse-grain KF for the MET-pIRIR250 signals. Fig. 4B showed an obvious De plateau between the stimulation temperature of 250 and 290°C, and a continuous increase from 50°C to 200°C. Fig. 4C-4F suggested a saturate dose of beyond 1200 Gy for the MET-pIRIR250 signals, while that of the MET-pIRIR290 signals is lower (Fig. 4C). Fig. 4D also illustrated that the DRCs of MET-pIRIR250 derived from different aliquots are similar to their SGC derived from 3–4 DRCs for each sample, suggesting that the SGC method (Roberts and Duller, 2004; Lai and Ou, 2013) could be applied for these samples.

Fig. 2

Yardang landform and sampling sections. The filled red circles denote the positions of sampling.

Fig. 3

Dose recovery test for MET-pIRIR protocols (A) and two-step pIRIR protocols (B).

Fig. 4

Luminescence properties of MET-pIRIR signals using the protocol in Table 2a: (A) Decay curves of K-feldspars and polyminerals, (B) Des at different stimulation temperatures and (C) corresponding DRCs for sample YD9-B, (D) DRCs of MET-pIRIR250 signals of sample YD8-B and their SGC. (E) DRC of MET-pIRIR250 signal of sample of field saturation in the QB, using two exponentials function. (F) Saturate ratio. It is expressed by the ratios of (Ln/Tn) (natural signals) and (Ls/Tn), the latter is derived from ~1969 Gy and field saturated dose for fine-grain polyminerals and coarse-grain K-feldspars, respectively (no fine-grain sample of field saturation were collected).

Bleaching behaviour and residuals

To test the bleaching behaviour of MET-pIRIR signals of the paleo-lacustrine sediments, six groups of small aliquots were exposed to natural sunlight for different bleaching durations in Linyi (118°17′ E, 35°07′ N) in August 2018. The results (Fig. 5) indicated that the residual doses of MET-pIRIR signals at different stimulation temperatures all decreased with the increase of bleaching time. Moreover, residual signals of 250°C were bleached to 4.2% of the natural signals after 3 hrs bleaching, and the residual dose dropped to only 21.8 Gy (equal to ca. 6.2 ka with an average dose rate of 3.5 Gy/ka) after 24 hrs. This suggested the MET-pIRIR250 signals could be well bleached in the QB, where the insolation is of over 5000 MJ/ (m2·a), 50–100% higher than in the low-altitude areas of the same latitude (Zheng and Zhao, 2017).

Fig. 5

Residual doses as a function of sunlight bleaching time for the MET-pIRIR signals of sample YD9-B.

Two-step pIRIR

To decrease the influence of the undetectable carryover charge (Kars et al., 2014) and probable anomalous fading, an extended stimulation time of 500 s and a big test dose of 248 Gy were applied (Colarossi et al., 2018). The latter has the effect of increasing D0 values as well (Qin and Zhou, 2012; Colarossi et al., 2018). The protocol for pIR50IR250 determined by dose recovery test was shown in Table 2b.

Dose recovery test and luminescence properties

Twenty aliquots of sample YD9-B were bleached by sunlight for 24 hrs for dose recovery test. Preheat temperatures of 250–320°C (250, 280, 300, and 320°C) were applied, followed by a first IR stimulation at 50°C, and a second IR stimulation at 225, 250, 270, and 290°C, respectively. The first dose of 620 Gy was given, and 3–4 aliquots for each temperature were measured. Without the subtraction of residual doses (for details see Section 4 – Two-step pIRIR – Residuals and anomalous fading test) from Des, the measured/given dose ratios (Fig. 3B) suggest the results of pIR50IR250 and pIR50IR270 are acceptable. Another dose recovery test of 992 Gy (Fig. 3B) and the smaller residual dose further confirmed that the pIR50IR250 signals behaved better.

The signals of the nature dose and test dose of the pIR50IR250 signals can decay to a low level after stimulation of 500 s (Fig. 6A), which was further confirmed by the relative stable sensitivity changes during the SAR cycles (Fig. 6C). Fig. 6B displayed that the natural dose of IRSL50 is much smaller than the pIR50IR250, which was attributed to the fading of the IRSL50. The SGC of the pIR50IR250 signals coincide with their DRCs as well.

Fig. 6

Luminescence properties of two-step pIRIR signals. (A) Decay curves of IR50IR250 signals, (B) DRCs and natural doses of IRSL50 and IR50IR250, and (C) Sensitivity changes of pIR50IR250 for sample YD9-B.

Residuals and anomalous fading test

The residual dose determination was conducted on six sunlight-bleached (24 hrs) aliquots for each temperature, and the results of pIR50IR225, pIR50IR250, pIR50IR270 and pIR50IR290 were 6.2, 8.2, 11.6, and 14.2 Gy, respectively. The anomalous fading rate measurements were conducted on three measured aliquots (YD9-B), and the single aliquot measurement procedures were similar to Auclair et al. (2003), but based on the pIR50IR250 protocol (Table 2b). The same regenerative dose of 124 Gy followed by a preheat of 280°C was given before different storage times. Using the software of Analyst, a series of Lx/Tx values as a function of storage times were plotted for the g-value that is normalised to a tc of 2 days (Huntley and Lamothe 2001). As shown in Fig. 7A and 7B, the measurements of 3 aliquots show a mean g-values of 1.54±0.20 %/decade for the pIR50IR250, and 2.97±0.66 %/decade for the IRSL50.

Fig. 7

Fading test of IRSL50 (A) and pIR50IR250 (B) signals of sample YD9-B, and Comparison of multiple age results (C).

Results and discussion
Comparisons of MET-pIRIR250 and pIR50IR250 dating
MET-pIRIR250

For MET-pIRIR, a plateau of similar De values obtained at higher temperatures could suggest negligible anomalous fading (Li and Li, 2011). In this study, the De plateaus between 250 and 290°C (Fig. 4C) suggested negligible fading as well. The MET-pIRIR250 signal was chosen because its residual dose was smaller and the signal level was higher than that of the MET-pIRIR290.

The measured residual dose of MET-pIRIR250, 21.8 Gy, (Fig. 5) was subtracted from the mean Des of each sample for correction. In this study, any aliquots without De plateau between MET-pIRIR250 and MET-pIRIR290, which suggested insufficient bleaching (Fu, 2014), were rejected. Furthermore, the DRCs fitted with double exponentials (Fig. 4D) can offer higher saturate dose of beyond 1200 Gy for MET-pIRIR250 signals. This was supported by the conclusion of Galbraith and Roberts (2012) that much higher De values could be estimated when the DRC was fitted accurately. A field saturated yardang sample offered a De of beyond 2237 Gy (Fig. 4E), suggesting the fading of the MET-pIRIR250 signals was very minimal. If the normalised natural signals of the saturate sample (Ls/Tn=3.961) was regarded as the saturation level, the normalised natural signals (Ln/Tn) could be compared with it to evaluate the saturate ratio ((Ln/Tn)/(Ls/Tn)) for each coarse-grained aliquot (Fig. 4F). Due to the lack of field saturate sample for fine grains, the minimal laboratory saturation level (~1969 Gy, we did not make the DRC saturation) was used to estimate a maximal saturate ratio for each fine-grained aliquot. Most of the coarse-grain samples have the saturate ratios of below 85%. However, without independent age control, we are cautious with the results of ca. 900– 1000 Gy. The success of dose recovery test of 895 Gy (Fig. 3A) further suggested that at least the results below 900 Gy were reliable. The comparison of the ages, stratigraphy and elevations among different sections also demonstrated the reliability of most of these ages, as interpreted in part 5.2. All the MET-pIRIR250 ages are in Table 1.

pIR50IR250

The fading test (Fig. 7A-7B) offered a mean g-value of 1.54±0.20 %/decade for pIR50IR250 signals. Some studies proposed that the fading correction for the pIR50IR225290 is unnecessary because either their natural signals can reach saturate level (Thiel et al., 2011; Liu et al., 2016), or the uncorrected age could agree with the independent ages (Thiel et al., 2011; Roberts, 2012). Thiel et al. (2011) proposed that the measured g-values (0.07±0.78 to 2.00±0.64 %/decade) for pIR50IR290 were artificial in the laboratory and should be ignored. In contrast, Li and Li (2012) found that the anomalous fading would lead to underestimations for older samples (e.g., >500 Gy) with the pIR50IR290 method, while it is not a problem for younger samples. For our samples, the measured ages of pIR50IR250 were severely underestimated by even more than 20% compared to MET-pIRIR250 ages. Based on the anomalous fading tests, ages of IRSL50 and pIR50IR250 were calibrated according to the model of Huntley (2006) for our relative old samples. The calculations were conducted with the R. luminescence package (Kreutzer et al., 2019), using the approaches in Kars et al. (2008) (a single-saturating exponential fit, 1EXP) and Guralnik et al. (2015) (a general-order kinetic fit, GOK), which had been evaluated for the fading-correction by King et al. (2018). The corrected results were shown in Fig. 7C, and Table 3 gives some details, including the samples’ saturation level (i.e., (n/N) is the samples’ level of saturation for the natural state; (n/N)_SS is the samples’ level of saturation for field steady-state (King et al. 2018)), measured De, corrected D0, corrected De, corrected age. The comparisons of saturation level displayed that when the measured Des of pIR50IR250 reach ~700–800 Gy, results of 1EXP fitting showed saturation (e.g., sample YD6-B, YD7-C and YD8-B), but not GOK fitting (Table 3). This suggested that the fitting mode might affect the saturation of simulated DRCs, especially for old samples. Nevertheless, YD7-B and YD9-B can be determined to be unsaturated (Table 3), which confirms that such high underestimation of pIR50IR250 was caused by anomalous fading rather than natural saturation. This agrees with the result of Thomsen et al. (2011) that the extended duration of the prior IRSL50 for beyond 100 s could not offer a significantly more stable pIR50IR290 signal. As shown in Fig. 7C, the ages of corrected IRSL50 agreed with MET-pIRIR250, however, except for YD7-B, the fading corrections of pIR50IR250 showed an overestimation (Fig. 7C), similar to the description of King et al. (2018). It might be related to a state near or already saturated (e.g. sample YD6-B, YD7-C and YD8-B), fitting modes and/or the differences between laboratory dose response and natural dose response caused by different origins or chemical compositions (King et al., 2018). As a result, the pIR50IR250 dating is affected by anomalous fading for our samples even for a prior IRSL50 of 500 s, and the correction for anomalous fading needs further studies. Consequently, the chronology for the following discussion was based on the MET-pIRIR250 ages.

The results corrected by Huntley (2006) method.

IRSL50
FunctionSample(n/N)(n/N)_SSMeasured Dea (Gy)Corrected D0b (Gy)Corrected Dec (Gy)Corrected Age d (ka)
YD6-B0.54±0.020.60±0.13397±16372±1973±124240±34
YD7-B0.43±0.010.58±0.14345±11465±1642±29229.0±19
1EXPYD7-C0.52±0.020.59±0.13429±18422±1981±85236±25.8
YD8-B0.48±0.010.57±0.14427±14479±1886±49330±29
YD9-B0.44±0.010.59±0.14364±10467±1700±27271±21
YD6-B0.46±0.020.60±0.17401±20362±11040±110256±32
YD7-B0.37±0.010.60±0.16345±12501±2673±30240±19
GOKYD7-C0.34±0.010.62±0.15423±21463±31070±82257±26
YD8-B0.40±0.010.57±0.12428±17494±1945±59352±32
YD9-B0.32±0.010.59±0.12365±11583±1733±31284±23
IR50IR250
FunctionSample(n/N)(n/N)_SSMeasured Dea (Gy)Corrected D0b (Gy)Corrected Dec (Gy)Corrected Age d (ka)
YD6-B0.72±0.020.72±0.21716±40439±11440±2334355±62
YD7-B0.57±0.020.71±0.2491±18483±1705±33252±21
1EXPYD7-C0.73±0.020.72±0.2815±48487±11744±328419±84
YD8-B0.69±0.020.71±0.2726±36497±21286±151480±65
YD9-B0.61±0.020.71±0.19616±23535±2920±46357±30
YD6-B0.54±0.020.72±0.19760±42485±21342±133331±40
YD7-B0.41±0.010.72±0.22500±20605±3731±32261±21
GOKYD7-C0.31±0.010.72±0.23862±54800±111497±102360±34
YD8-B0.52±0.020.71±0.19766±45549±21300±98484±49
YD9-B0.24±0.010.72±0.24633±281170±26957±39371±29

a. De calculated through measured DRC (King et al., 2018).

b. D0 for simulated natural DRC (King et al., 2018).

c. De calculated through simulated natural DRC (King et al., 2018).

d. Age calculated through simulated natural DRC (King et al., 2018).

pIRIR chronology for paleo-lacustrine sediments

Previous chronology of lacustrine sediments in the QB was mainly based on 14C dating during the past decades (e.g., Chen et al., 1981; Chen and Bowler, 1986; Bowler et al., 1986; Zhang et al., 2008). A mega-Qaidam paleolake was proposed to exist during ca. 40–30 ka (MIS3) based on the 14C dating of shells in the shell-bar (Fig. 1B, 2703 m a.s.l. on Google Earth) in the southeastern QSL region (Chen and Bowler, 1986; Zhang et al., 2008). However, the range of 14C dating is too young for the yardangs in the QB, and even the 14C ages of 25–40 ka were proved to be underestimated in the QB (Yu et al., 2009; Lai et al., 2014; Mischke et al., 2015; Yu et al., 2018). Lai et al. (2014) dated the shell-bar to MIS5 (~100–110 ka) based on quartz OSL. While the upper dating limit of quarts OSL (ca. 150 Gy on the CLP (Buylaert et al., 2008; Chapot et al., 2012)) implied that this result might also be underestimated. The feldspar MET-pIRIR250, in this study, offered seven paleo-lacustrine ages ranged from ca. 200 to 340 ka in the northern QSL region (Table 1), demonstrating a mega-Qaidam paleo-lake existed in QSL during and prior to MIS 7.

Fig. 8

(A) Scatter diagram of lacustrine ages against altitudes. (B) Probability density of lacustrine ages. (C) The composite δ 18O record of stalagmites (Cheng et al., 2016). (D) Insolation at 30° N (Berger and Loutre, 1991). (E) Composite sea level stack (Spratt and Lisiecki, 2016).

The new MET-pIRIR250 ages from this paper, together with the elevations of sections and samples, were displayed in Fig. 1C. The purpose of this study is to explore the termination time of the lacustrine environment. Consequently, we tried to investigate the ages of the highest yardangs in different regions. Based on the distribution, stratigraphy and ages, the five sections could be classified as three regions, the northern region (YD3), middle region (YD6 and YD7) and the eastern region. The YD6 and YD7 sections are close in distance and elevation. The De of YD7-B was only 673 Gy, which was far from saturation (Fig. 4D-4F), and consequently, its age of 240±16 ka is considered reliable. The YD6 section, at a higher elevation than YD7, should be younger than the latter. The YD6 presented similar ages with YD7 (reverse, but the same within errors), and we took their average age of 223±20 ka. As a result, the termination of the lacustrine environment in the middle region was after 220 ka. This also agrees with the YD3 section in higher elevation and with younger ages (201±25 ka). In this case, we can conclude that the lacustrine environment in the middle and northern regions terminated after ca. 200 ka, the MIS7. The low De of YD7-B further suggested these similar ages on similar elevation were less affected by fading and reliable. The YD8 and YD9 sections located at a higher elevation, and the De of YD9-B, 790 Gy, suggested the ages of MIS 9 should also be reliable. However, the samples cannot well present the latest time of lakes because they were not taken from the top of the yardangs, and consequently, it is unnecessary to make much interpretation on these two samples here.

Implications for yardang development

Taking into account that the previous radiocarbon ages (MIS3, Chen and Bowler, 1986; Zhang et al., 2008) and quartz OSL ages (MIS5, Lai et al., 2014) of the palaeo-lacustrine sediments are possible to be underestimated (Yu et al., 2009; Lai et al., 2014; Mischke et al., 2015; Yu et al., 2018; Buylaert et al., 2008; Chapot et al., 2012), there is no robust chronological evidence supporting the existence of mega-Qaidam paleolake since MIS6 at present. Additionally, the large-scale expansion of the Tiekui Dunefield (Fig. 1B), at the eastern end of the QB, suggested that there should be no mega lake in the QB during the most time from MIS6 to the early Holocene (Yu et al., 2019). Even during MIS5, when the climate should be relatively humid, there were still dune activities during MIS5d and MIS5b (Yu et al., 2019). Therefore, it is reasonable to infer that the mega-lake maintained till MIS7, and the severe wind-erosion and the widespread yardang formation in the QSL region started since MIS6. The eroded materials should have contributed to the expansions of the Tiekui Dunefield in the downwind direction of the QB since MIS6 (Yu et al., 2019). The mega-Qaidam Lake demonstrated a humid climate during MIS7, while the severe wind erosion of yardangs and the expansion of the Tiekui Dunefield both indicated arid and windy climate during MIS6. The comparisons among lacustrine ages (Fig. 8A-8B), δ18O records of stalagmites in Asain Summer Monsoon (ASM) influenced region (Fig. 8C, Cheng et al., 2016), summer insolation of 30°N (Fig. 8D, Berger and Loutre, 1991), and sea level changes (Fig. 8E, Spratt and Lisiecki, 2016) suggested the mega-Qaidam Lake developed under the warm and humid climate during MIS7, while the transition to arid climate might result from the retreat of ASM and strengthening of the westerlies (An et al., 2012) during MIS6. This suggested the palaeoenvironmental changes in glacial-interglacial scale in the QB, however, these limited data were not sufficient to support further discussions about the relevant mechanisms and processes, and more detailed studies are needed in future.

Conclusions

Two main conclusions were drawn from this study: one is to find a suitable dating method, and the other is to infer the geomorphic processes based on the new ages. Methodology study suggests that the pIRIR dating is suitable for the paleo-lacustrine sediments in the QB, for both fine-grained polymineral samples and coarse-grain KF. The MET-pIRIR250 signals could be well bleached and were less affected by fading as demonstrated by a De plateau. For pIR50IR250, fading correction is necessary, but the correction method for such old samples needs further studies. Thus, the results of MET-pIRIR250 dating were used to explore the termination time of the lacustrine environment.

For the geomorphic processes of the yardang formation, the ages of ~200–340 ka from lacustrine sediment reveal that the mega-Qaidam paleolake existed during and prior to MIS7. The most recent extensive formation of yardangs in the northern QSL region might start since MIS6.

Fig. 1

Landform (A-B) and sampled yardangs (C-D) in the Qaidam Basin. The elevations measured by differential GPS were used in Fig. 1C as it's more accurate.
Landform (A-B) and sampled yardangs (C-D) in the Qaidam Basin. The elevations measured by differential GPS were used in Fig. 1C as it's more accurate.

Fig. 2

Yardang landform and sampling sections. The filled red circles denote the positions of sampling.
Yardang landform and sampling sections. The filled red circles denote the positions of sampling.

Fig. 3

Dose recovery test for MET-pIRIR protocols (A) and two-step pIRIR protocols (B).
Dose recovery test for MET-pIRIR protocols (A) and two-step pIRIR protocols (B).

Fig. 4

Luminescence properties of MET-pIRIR signals using the protocol in Table 2a: (A) Decay curves of K-feldspars and polyminerals, (B) Des at different stimulation temperatures and (C) corresponding DRCs for sample YD9-B, (D) DRCs of MET-pIRIR250 signals of sample YD8-B and their SGC. (E) DRC of MET-pIRIR250 signal of sample of field saturation in the QB, using two exponentials function. (F) Saturate ratio. It is expressed by the ratios of (Ln/Tn) (natural signals) and (Ls/Tn), the latter is derived from ~1969 Gy and field saturated dose for fine-grain polyminerals and coarse-grain K-feldspars, respectively (no fine-grain sample of field saturation were collected).
Luminescence properties of MET-pIRIR signals using the protocol in Table 2a: (A) Decay curves of K-feldspars and polyminerals, (B) Des at different stimulation temperatures and (C) corresponding DRCs for sample YD9-B, (D) DRCs of MET-pIRIR250 signals of sample YD8-B and their SGC. (E) DRC of MET-pIRIR250 signal of sample of field saturation in the QB, using two exponentials function. (F) Saturate ratio. It is expressed by the ratios of (Ln/Tn) (natural signals) and (Ls/Tn), the latter is derived from ~1969 Gy and field saturated dose for fine-grain polyminerals and coarse-grain K-feldspars, respectively (no fine-grain sample of field saturation were collected).

Fig. 5

Residual doses as a function of sunlight bleaching time for the MET-pIRIR signals of sample YD9-B.
Residual doses as a function of sunlight bleaching time for the MET-pIRIR signals of sample YD9-B.

Fig. 6

Luminescence properties of two-step pIRIR signals. (A) Decay curves of IR50IR250 signals, (B) DRCs and natural doses of IRSL50 and IR50IR250, and (C) Sensitivity changes of pIR50IR250 for sample YD9-B.
Luminescence properties of two-step pIRIR signals. (A) Decay curves of IR50IR250 signals, (B) DRCs and natural doses of IRSL50 and IR50IR250, and (C) Sensitivity changes of pIR50IR250 for sample YD9-B.

Fig. 7

Fading test of IRSL50 (A) and pIR50IR250 (B) signals of sample YD9-B, and Comparison of multiple age results (C).
Fading test of IRSL50 (A) and pIR50IR250 (B) signals of sample YD9-B, and Comparison of multiple age results (C).

Fig. 8

(A) Scatter diagram of lacustrine ages against altitudes. (B) Probability density of lacustrine ages. (C) The composite δ 18O record of stalagmites (Cheng et al., 2016). (D) Insolation at 30° N (Berger and Loutre, 1991). (E) Composite sea level stack (Spratt and Lisiecki, 2016).
(A) Scatter diagram of lacustrine ages against altitudes. (B) Probability density of lacustrine ages. (C) The composite δ 18O record of stalagmites (Cheng et al., 2016). (D) Insolation at 30° N (Berger and Loutre, 1991). (E) Composite sea level stack (Spratt and Lisiecki, 2016).

The results corrected by Huntley (2006) method.

IRSL50
FunctionSample(n/N)(n/N)_SSMeasured Dea (Gy)Corrected D0b (Gy)Corrected Dec (Gy)Corrected Age d (ka)
YD6-B0.54±0.020.60±0.13397±16372±1973±124240±34
YD7-B0.43±0.010.58±0.14345±11465±1642±29229.0±19
1EXPYD7-C0.52±0.020.59±0.13429±18422±1981±85236±25.8
YD8-B0.48±0.010.57±0.14427±14479±1886±49330±29
YD9-B0.44±0.010.59±0.14364±10467±1700±27271±21
YD6-B0.46±0.020.60±0.17401±20362±11040±110256±32
YD7-B0.37±0.010.60±0.16345±12501±2673±30240±19
GOKYD7-C0.34±0.010.62±0.15423±21463±31070±82257±26
YD8-B0.40±0.010.57±0.12428±17494±1945±59352±32
YD9-B0.32±0.010.59±0.12365±11583±1733±31284±23
IR50IR250
FunctionSample(n/N)(n/N)_SSMeasured Dea (Gy)Corrected D0b (Gy)Corrected Dec (Gy)Corrected Age d (ka)
YD6-B0.72±0.020.72±0.21716±40439±11440±2334355±62
YD7-B0.57±0.020.71±0.2491±18483±1705±33252±21
1EXPYD7-C0.73±0.020.72±0.2815±48487±11744±328419±84
YD8-B0.69±0.020.71±0.2726±36497±21286±151480±65
YD9-B0.61±0.020.71±0.19616±23535±2920±46357±30
YD6-B0.54±0.020.72±0.19760±42485±21342±133331±40
YD7-B0.41±0.010.72±0.22500±20605±3731±32261±21
GOKYD7-C0.31±0.010.72±0.23862±54800±111497±102360±34
YD8-B0.52±0.020.71±0.19766±45549±21300±98484±49
YD9-B0.24±0.010.72±0.24633±281170±26957±39371±29

Age results of MET-pIRIR250 with sample informations.

(a) MET-pIRIR250 of Feldspar(b) pIR50IR250 of Feldspar
StepTreatmentMeasuredTreatmentMeasured
1Dose-Dose-
2Preheat 320°C for 60 s-Preheat 280°C for 60 s-
3IRSL 50°C for 100 s-IRSL 50°C for 500 s-
4IRSL 100°C for 100 s-IRSL 250˚C for 500 sLx
5IRSL 150°C for 100 s-Test dose-
6IRSL 200°C for 100 s-Preheat 280°C for 60 s-
7IRSL 250°C for 100 sLxIRSL 50°C for 500 s-
8IRSL 290°C for 100 s-IRSL 250˚C for 500 sTx
9Test dose-Return to step 1
10Preheat 320°C for 60 s-
11IRSL 50°C for 100 s-
12IRSL 100°C for 100 s-
13IRSL 150°C for 100 s-
14IRSL 200°C for 100 s-
15IRSL 250°C for 100 sTx
16IRSL 290°C for 100 s-
17IRSL 320°C for 100 s-
18Return to step 1

Al-Dousari AM, Al-Elaj M, Al-Enezi E and Al-Shareeda A, 2009. Origin and characteristics of yardangs in the Um Al-Rimam depressions (N Kuwait). Geomorphology 104: 93–104, DOI 10.1016/j.geomorph.2008.05.010.Al-DousariAMAl-ElajMAl-EneziEandAl-ShareedaA2009Origin and characteristics of yardangs in the Um Al-Rimam depressions (N Kuwait)Geomorphology1049310410.1016/j.geomorph.2008.05.010Open DOISearch in Google Scholar

An Z, Colman SM, Zhou W, Li X, Brown ET, Jull AJT, Cai Y, Huang Y, Lu X, Chang H, Song Y, Sun Y, Xu H, Liu W, Jin Z, Liu X, Cheng P, Liu Y, Ai L, Li X, Liu X, Yan L, Shi Z, Wang X, Wu F, Qiang X, Dong J, Lu F and Xu X, 2012. Interplay between the Westerlies and Asian monsoon recorded in Lake Qinghai sediments since 32 ka. Scientific Reports 2: 619, DOI 10.1038/srep00619.AnZColmanSMZhouWLiXBrownETJullAJTCaiYHuangYLuXChangHSongYSunYXuHLiuWJinZLiuXChengPLiuYAiLLiXLiuXYanLShiZWangXWuFQiangXDongJLuFandXuX2012Interplay between the Westerlies and Asian monsoon recorded in Lake Qinghai sediments since 32 kaScientific Reports261910.1038/srep00619Open DOISearch in Google Scholar

Anglés A and Li YL, 2017. The western Qaidam Basin as a potential Martian environmental analogue: an overview. Journal of Geophysical Research: Planets 122: 856–888, DOI 10.1002/2017JE005293.AnglésAandLiYL2017The western Qaidam Basin as a potential Martian environmental analogue: an overviewJournal of Geophysical Research: Planets12285688810.1002/2017JE005293Open DOISearch in Google Scholar

Auclair M, Lamothe M and Huot S, 2003. Measurement of anomalous fading for feldspar IRSL using SAR. Radiation Measurements 37(4–5): 487–492, DOI 10.1016/s1350-4487(03)00018-0.AuclairMLamotheMandHuotS2003Measurement of anomalous fading for feldspar IRSL using SARRadiation Measurements374–548749210.1016/s1350-4487(03)00018-0Open DOISearch in Google Scholar

Balescu S and Lamothe M, 1994. Comparison of TL and IRSL age estimates of feldspar coarse grains from waterlain sediments. Quaternary Science Reviews 13(5–7): 437–444, DOI 10.1016/0277-3791(94)90056-6.BalescuSandLamotheM1994Comparison of TL and IRSL age estimates of feldspar coarse grains from waterlain sedimentsQuaternary Science Reviews135–743744410.1016/0277-3791(94)90056-6Open DOISearch in Google Scholar

Berger A and Loutre MF, 1991. Insolation values for the climate of the last 10 million years. Quaternary Science Reviews 10(4): 297–317, DOI 10.1016/0277-3791(91)90033-Q.BergerAandLoutreMF1991Insolation values for the climate of the last 10 million yearsQuaternary Science Reviews10429731710.1016/0277-3791(91)90033-QOpen DOISearch in Google Scholar

Bowler JM, Chen KZ and Yuan BY, 1987. Systematic variations in loess source areas: Evidence from Qaidam and Qinghai basins, western China, in Tungsheng, L., ed., Aspects of Loess Research. China Ocean Press, Beijing: 39–51.BowlerJMChenKZandYuanBY1987Systematic variations in loess source areas: Evidence from Qaidam and Qinghai basins, western ChinainTungshengL.edAspects of Loess ResearchChina Ocean PressBeijing3951Search in Google Scholar

Bowler JM, Huang Q, Chen KZ, Head MJ and Yuan BY, 1986. Radiocarbon dating of playa-lake hydrologic changes: Examples from northwestern China and central Australia. Palaeogeography, Palaeoclimatology, Palaeoecology 54: 241–260, DOI 10.1016/0031-0182(86)90127-6.BowlerJMHuangQChenKZHeadMJandYuanBY1986Radiocarbon dating of playa-lake hydrologic changes: Examples from northwestern China and central AustraliaPalaeogeography, Palaeoclimatology, Palaeoecology5424126010.1016/0031-0182(86)90127-6Open DOISearch in Google Scholar

Buylaert JP, Murray AS, Thomsen KJ and Jain M, 2009. Testing the potential of an elevated temperature IRSL signal from K-feldspar. Radiation Measurements 44: 560–565, DOI 10.1016/j.radmeas.2009.02.007.BuylaertJPMurrayASThomsenKJandJainM2009Testing the potential of an elevated temperature IRSL signal from K-feldsparRadiation Measurements4456056510.1016/j.radmeas.2009.02.007Open DOISearch in Google Scholar

Buylaert JP, Murray AS, Vandenberghe D, Vriend M, Corte FD and Haute PVD, 2008. Optical dating of Chinese loess using sand-sized quartz: Establishing a time frame for Late Pleistocene climate changes in the western part of the Chinese Loess Plateau. Quaternary Geochronology 3(1–2): 99–113, DOI 10.1016/j.radmeas.2009.02.007.BuylaertJPMurrayASVandenbergheDVriendMCorteFDandHautePVD2008Optical dating of Chinese loess using sand-sized quartz: Establishing a time frame for Late Pleistocene climate changes in the western part of the Chinese Loess PlateauQuaternary Geochronology31–29911310.1016/j.radmeas.2009.02.007Open DOISearch in Google Scholar

Chapot MS, Roberts HM, Duller GAT and Lai ZP, 2012. A comparison of natural- and laboratory-generated dose response curves for quartz optically stimulated luminescence signals from Chinese Loess. Radiation Measurements 47(11–12): 1045–1052, DOI 10.1016/j.radmeas.2012.09.001.ChapotMSRobertsHMDullerGATandLaiZP2012A comparison of natural- and laboratory-generated dose response curves for quartz optically stimulated luminescence signals from Chinese LoessRadiation Measurements4711–121045105210.1016/j.radmeas.2012.09.001Open DOISearch in Google Scholar

Chen KZ and Bowler JM, 1985. Study on sedimentary characteristics and paleoclimate evolution of qarhan salt lake in Qaidam Basin. Science China: series B 5: 79–89 (in Chinese).ChenKZandBowlerJM1985Study on sedimentary characteristics and paleoclimate evolution of qarhan salt lake in Qaidam BasinScience China: series B57989(in Chinese)Search in Google Scholar

Chen KZ and Bowler JM, 1986. Late pleistocene evolution of salt lakes in the Qaidam basin, Qinghai province, China. Palaeogeography, Palaeoclimatology, Palaeoecology 54: 87–104, DOI 10.1016/0031-0182(86)90119-7.ChenKZandBowlerJM1986Late pleistocene evolution of salt lakes in the Qaidam basin, Qinghai province, ChinaPalaeogeography, Palaeoclimatology, Palaeoecology548710410.1016/0031-0182(86)90119-7Open DOISearch in Google Scholar

Chen KZ, Yang S and Zheng X, 1981. The salt lakes on the Qinghai-Xizang plateau. Acta Geographica Sinica 36(1): 13–21 (in Chinese with English abstract).ChenKZYangSandZhengX1981The salt lakes on the Qinghai-Xizang plateauActa Geographica Sinica3611321(in Chinese with English abstract)Search in Google Scholar

Cheng H, Edwards RL, Sinha A, Spötl C, Yi L, Chen ST, Kelly M, Kathayat G, Wang XF, Li XL, Kong XG, Wang YX, Ning YF and Zhang HW, 2016. The asian monsoon over the past 640,000 years and ice age terminations. Nature 534(7609): 640–646, DOI 10.1038/nature18591.ChengHEdwardsRLSinhaASpötlCYiLChenSTKellyMKathayatGWangXFLiXLKongXGWangYXNingYFandZhangHW2016The asian monsoon over the past 640,000 years and ice age terminationsNature534760964064610.1038/nature18591Open DOISearch in Google Scholar

Colarossi D, Duller GAT and Roberts HM, 2018. Exploring the behaviour of luminescence signals from feldspars: Implications for the single aliquot regenerative dose protocol. Radiation Measurements 109: 35–44, DOI 10.1016/j.radmeas.2017.07.005.ColarossiDDullerGATandRobertsHM2018Exploring the behaviour of luminescence signals from feldspars: Implications for the single aliquot regenerative dose protocolRadiation Measurements109354410.1016/j.radmeas.2017.07.005Open DOISearch in Google Scholar

Durcan JA, King GE and Duller GAT, 2015. DRAC: Dose Rate and Age Calculator for trapped charge dating. Quaternary Geochronology 28: 54–61, DOI 10.1016/j.quageo.2015.03.012.DurcanJAKingGEandDullerGAT2015DRAC: Dose Rate and Age Calculator for trapped charge datingQuaternary Geochronology28546110.1016/j.quageo.2015.03.012Open DOISearch in Google Scholar

Fu X, 2014. The D e (T, t) plot: A straightforward self-diagnose tool for post-IR IRSL dating procedures. Geochronometria 41: 315–326, DOI 10.2478/s13386-013-0167-9.FuX2014The D e (T, t) plot: A straightforward self-diagnose tool for post-IR IRSL dating proceduresGeochronometria4131532610.2478/s13386-013-0167-9Open DOISearch in Google Scholar

Galbraith RF and Roberts RG, 2012. Statistical aspects of equivalent dose and error calculation and display in OSL dating: An overview and some recommendations. Quaternary Geochronology, 11: 1–27, DOI 10.1016/j.quageo.2012.04.020.GalbraithRFandRobertsRG2012Statistical aspects of equivalent dose and error calculation and display in OSL dating: An overview and some recommendationsQuaternary Geochronology1112710.1016/j.quageo.2012.04.020Open DOISearch in Google Scholar

Guralnik B, Li B, Jain M, Chen R, Paris RB, Murray AS, Li SH, Pagonis P and Herman F, 2015. Radiation-induced growth and isothermal decay of infrared-stimulated luminescence from feldspar. Radiation Measurements 81: 224–231, DOI 10.1016/j.radmeas.2015.02.011.GuralnikBLiBJainMChenRParisRBMurrayASLiSHPagonisPandHermanF2015Radiation-induced growth and isothermal decay of infrared-stimulated luminescence from feldsparRadiation Measurements8122423110.1016/j.radmeas.2015.02.011Open DOISearch in Google Scholar

Goudie AS, 2007. Mega-Yardangs: A Global Analysis. Geography Compass 1(1): 65–81, DOI 10.1111/j.1749-8198.2006.00003.x.GoudieAS2007Mega-Yardangs: A Global AnalysisGeography Compass11658110.1111/j.1749-8198.2006.00003.xOpen DOISearch in Google Scholar

Halimov M and Fezer F, 1989. Eight yardang types in central Asia. Zeitschrift Fur Geomorphologie 33: 205–217.HalimovMandFezerF1989Eight yardang types in central AsiaZeitschrift Fur Geomorphologie33205217Search in Google Scholar

Hu CQ, Chen NH, Kapp P, Chen J, Xiao A and Zhao Y, 2017. Yardang geometries in the Qaidam Basin and their controlling factors. Geomorphology 299: 142–151, DOI 10.1016/j.geomorph.2017.09.029.HuCQChenNHKappPChenJXiaoAandZhaoY2017Yardang geometries in the Qaidam Basin and their controlling factorsGeomorphology29914215110.1016/j.geomorph.2017.09.029Open DOISearch in Google Scholar

Huntley DJ, 2006. An explanation of the power-law decay of luminescence. Journal of Physics: Condensed Matter 18(4): 1359–1365, DOI 10.1088/0953-8984/18/4/020.HuntleyDJ2006An explanation of the power-law decay of luminescenceJournal of Physics: Condensed Matter1841359136510.1088/0953-8984/18/4/020Open DOISearch in Google Scholar

Huntley DJ and Baril MR, 1997. The K content of the K-feldspars being measured in optical dating or in thermoluminescence dating. Ancient TL 15: 11–13.HuntleyDJandBarilMR1997The K content of the K-feldspars being measured in optical dating or in thermoluminescence datingAncient TL151113Search in Google Scholar

Huntley DJ and Lamothe M, 2001. Ubiquity of anomalous fading in K-feldspars and the measurement and correction for it in optical dating. Canadian Journal of Earth Sciences 38(7): 1093–1106, DOI 10.1139/cjes-38-7-1093.HuntleyDJandLamotheM2001Ubiquity of anomalous fading in K-feldspars and the measurement and correction for it in optical datingCanadian Journal of Earth Sciences3871093110610.1139/cjes-38-7-1093Open DOISearch in Google Scholar

Kapp P, Pelletier JD, Rohrmann A, Heermance R, Russell J and Ding L, 2011. Wind erosion in the Qaidam basin, central Asia: Implications for tectonics, paleoclimate, and the source of the Loess Plateau. Geological Society of America Today 21(4–5): 4–10, DOI 10.1130/GSATG99A.1.KappPPelletierJDRohrmannAHeermanceRRussellJandDingL2011Wind erosion in the Qaidam basin, central Asia: Implications for tectonics, paleoclimate, and the source of the Loess PlateauGeological Society of America Today214–541010.1130/GSATG99A.1Open DOISearch in Google Scholar

Kars RH, Reimann T and Wallinga J, 2014. Are feldspar SAR protocols appropriate for post-IR IRSL dating? Quaternary Geochronology 22: 126–136, DOI 10.1016/j.quageo.2014.04.001.KarsRHReimannTandWallingaJ2014Are feldspar SAR protocols appropriate for post-IR IRSL dating?Quaternary Geochronology2212613610.1016/j.quageo.2014.04.001Open DOISearch in Google Scholar

Kars RH, Wallinga J and Cohen KM, 2008. A new approach towards anomalous fading correction for feldspar IRSL dating – tests on samples in field saturation. Radiation Measurements 43(2–6): 786–790, DOI 10.1016/j.radmeas.2008.01.021.KarsRHWallingaJandCohenKM2008A new approach towards anomalous fading correction for feldspar IRSL dating – tests on samples in field saturationRadiation Measurements432–678679010.1016/j.radmeas.2008.01.021Open DOISearch in Google Scholar

King GE, Christoph B, Roberts HM, and Pearceb NJG, 2018. Age determination using feldspar: Evaluating fading-correction model performance. Radiation Measurements 119: 58–73, DOI 10.1016/j.radmeas.2018.07.013.KingGEChristophBRobertsHMandPearcebNJG2018Age determination using feldspar: Evaluating fading-correction model performanceRadiation Measurements119587310.1016/j.radmeas.2018.07.013Open DOISearch in Google Scholar

Kreutzer S, Burow C, Dietze M, Fuchs MC, Schmidt C, Fischer M and Friedrich J, 2019. Luminescence: Comprehensive Luminescence Dating Data Analysis. R package version 0.9.0.109. https://CRAN.R-project.org/package=LuminescenceKreutzerSBurowCDietzeMFuchsMCSchmidtCFischerMandFriedrichJ2019Luminescence: Comprehensive Luminescence Dating Data AnalysisR package version0.9.0.109https://CRAN.R-project.org/package=LuminescenceSearch in Google Scholar

Lai ZP, Mischke S and Madsen DB, 2014. Paleoenvironmental implications of new OSL dates on the formation of the “Shell Bar” in the Qaidam Basin, northeastern Qinghai-Tibetan Plateau. Journal of Paleolimnology 51: 197–210, DOI 10.1007/s10933-013-9710-1.LaiZPMischkeSandMadsenDB2014Paleoenvironmental implications of new OSL dates on the formation of the “Shell Bar” in the Qaidam Basin, northeastern Qinghai-Tibetan PlateauJournal of Paleolimnology5119721010.1007/s10933-013-9710-1Open DOISearch in Google Scholar

Lai ZP and Ou XJ, 2013. Basic procedures of optically stimulated luminescence (OSL) dating. Progress in Geography 32(5): 683– 693 (in Chinese with English abstract), DOI 10.11820/dlkxjz.2013.05.001.LaiZPandOuXJ2013Basic procedures of optically stimulated luminescence (OSL) datingProgress in Geography325683693(in Chinese with English abstract)10.11820/dlkxjz.2013.05.001Open DOISearch in Google Scholar

Li B and Li SH, 2011. Luminescence dating of K-feldspar from sediments: A protocol without anomalous fading correction. Quaternary Geochronology 6: 468–479, DOI 10.1016/j.quageo.2011.05.001.LiBandLiSH2011Luminescence dating of K-feldspar from sediments: A protocol without anomalous fading correctionQuaternary Geochronology646847910.1016/j.quageo.2011.05.001Open DOISearch in Google Scholar

Li B and Li SH, 2012. A reply to the comments by Thomsen et al. on “Luminescence dating of K-feldspar from sediments: A protocol without anomalous fading correction”. Quaternary Geochronology 8: 49–51, DOI 10.1016/j.quageo.2011.10.001.LiBandLiSH2012A reply to the comments by Thomsen et alon “Luminescence dating of K-feldspar from sediments: A protocol without anomalous fading correction”. Quaternary Geochronology8495110.1016/j.quageo.2011.10.001Open DOISearch in Google Scholar

Li GQ, Madsen DB, Jin M, Stevens T, Tao SX, She LL, Yang LP, Li FL, Wei HT, Duan YW and Chen FH, 2018. Orbital scale lake evolution in the Ejina Basin, central Gobi Desert, China revealed by K-feldspar luminescence dating of paleolake shoreline features. Quaternary International 482: 109–121, DOI 10.1016/j.quaint.2018.03.040.LiGQMadsenDBJinMStevensTTaoSXSheLLYangLPLiFLWeiHTDuanYWandChenFH2018Orbital scale lake evolution in the Ejina Basin, central Gobi Desert, China revealed by K-feldspar luminescence dating of paleolake shoreline featuresQuaternary International48210912110.1016/j.quaint.2018.03.040Open DOISearch in Google Scholar

Li JY, Dong ZB, Qian, GQ, Zhang ZC, Luo WY, Lu JF, Wang M, 2016. Yardangs in the Qaidam Basin, northwestern China: Distribution and morphology. Aeolian Research 20: 89–99, DOI 10.1016/j.aeolia.2015.11.002.LiJYDongZBQianGQZhangZCLuoWYLuJFWangM2016Yardangs in the Qaidam Basin, northwestern China: Distribution and morphologyAeolian Research20899910.1016/j.aeolia.2015.11.002Open DOISearch in Google Scholar

Liu JF, Murray AS, Buylaert JP, Jain M, Chen J and Lu YC, 2016. Stability of fine‐grained TT‐OSL and post‐IR IRSL signals from a c. 1 Ma sequence of aeolian and lacustrine deposits from the Nihewan Basin (northern China). Boreas 45(4): 703–714, DOI 10.1111/bor.12180.LiuJFMurrayASBuylaertJPJainMChenJandLuYC2016Stability of fine‐grained TT‐OSL and post‐IR IRSL signals from a c1 Ma sequence of aeolian and lacustrine deposits from the Nihewan Basin (northern China). Boreas45470371410.1111/bor.12180Open DOISearch in Google Scholar

Mischke S, Madsen D, Zhang CJ and Lai ZP, 2015. Reply to comment by Zhang (2014): The Shell Bar in the Qaidam Basin: fluvial or lake deposit, and OSL versus 14 C age data. Journal of Paleolimnology 53: 335–344, DOI 10.1007/s10933-014-9817-z.MischkeSMadsenDZhangCJandLaiZP2015Reply to comment by Zhang (2014): The Shell Bar in the Qaidam Basin: fluvial or lake deposit, and OSL versus 14 C age dataJournal of Paleolimnology5333534410.1007/s10933-014-9817-zOpen DOISearch in Google Scholar

Murray AS and Wintle AG, 2000. Luminescence dating of quartz using an improved singlealiquot regenerative-dose protocol. Radiation Measurements 32: 57–73, DOI 10.1016/s1350-4487(99)00253-x.MurrayASandWintleAG2000Luminescence dating of quartz using an improved singlealiquot regenerative-dose protocolRadiation Measurements32577310.1016/s1350-4487(99)00253-xOpen DOISearch in Google Scholar

Murray AS and Wintle AG, 2003. The single aliquot regenerative dose protocol: potential for improvements in reliability. Radiation Measurements 37: 377–381, DOI 10.1016/s1350-4487(03)00053-2.MurrayASandWintleAG2003The single aliquot regenerative dose protocol: potential for improvements in reliabilityRadiation Measurements3737738110.1016/s1350-4487(03)00053-2Open DOISearch in Google Scholar

Pullen A, Kapp P, Mccallister AT, Chang H, Gehrels G E, Garzione CN, Heermance RV and Ding L, 2011. Qaidam Basin and northern Tibetan Plateau as dust sources for the Chinese Loess Plateau and paleoclimatic implications. Geology 39(11): 1031–1034, DOI 10.1130/G32296.1.PullenAKappPMccallisterATChangHGehrelsG EGarzioneCNHeermanceRVandDingL2011Qaidam Basin and northern Tibetan Plateau as dust sources for the Chinese Loess Plateau and paleoclimatic implicationsGeology39111031103410.1130/G32296.1Open DOISearch in Google Scholar

Qin JT and Zhou LP, 2012. Effects of thermally transferred signals in the post-IR IRSL SAR protocol. Radiation Measurements 47: 710–715, DOI 10.1016/j.radmess.2011.12.011.QinJTandZhouLP2012Effects of thermally transferred signals in the post-IR IRSL SAR protocolRadiation Measurements4771071510.1016/j.radmess.2011.12.011Open DOISearch in Google Scholar

Rees-Jones J, 1995. Optical dating of young sediments using fine-grained quartz. Ancient TL 13: 9–14.Rees-JonesJ1995Optical dating of young sediments using fine-grained quartzAncient TL13914Search in Google Scholar

Roberts HM, 2012. Testing Post-IR IRSL protocols for minimising fading in feldspars, using Alaskan loess with independent chronological control. Radiation Measurements 47(9): 716–724, DOI 10.1016/j.radmeas.2012.03.022.RobertsHM2012Testing Post-IR IRSL protocols for minimising fading in feldspars, using Alaskan loess with independent chronological controlRadiation Measurements47971672410.1016/j.radmeas.2012.03.022Open DOISearch in Google Scholar

Roberts HM and Duller GAT, 2004. Standardised growth curves for optical dating of sediment using multiple-grain aliquots. Radiation Measurements 38: 241–252, DOI 10.1016/j.radmeas.2003.10.001.RobertsHMandDullerGAT2004Standardised growth curves for optical dating of sediment using multiple-grain aliquotsRadiation Measurements3824125210.1016/j.radmeas.2003.10.001Open DOISearch in Google Scholar

Rohrmann A, Heermance R, Kapp P and Cai FL, 2013. Wind as the primary driver of erosion in the Qaidam Basin, China. Earth and Planetary Science Letters 374: 1–10, DOI 10.1016/j.epsl.2013.03.011.RohrmannAHeermanceRKappPandCaiFL2013Wind as the primary driver of erosion in the Qaidam Basin, ChinaEarth and Planetary Science Letters37411010.1016/j.epsl.2013.03.011Open DOISearch in Google Scholar

Spratt RM and Lisiecki LE, 2016. A Late Pleistocene sea level stack. Climate of the Past 12: 1079–1092, DOI 10.5194/cp-12-1079-2016.SprattRMandLisieckiLE2016A Late Pleistocene sea level stackClimate of the Past121079109210.5194/cp-12-1079-2016Open DOISearch in Google Scholar

Sun YJ, Lai ZP, Long H, Liu XJ and Fan QS, 2010. Quartz OSL dating of archaeological sites in Xiao Qaidam Lake of the NE Qinghai-Tibetan Plateau and its implications for palaeoenvironmental-changes. Quaternary Geochronology 5(2): 360–364, DOI 10.1016/j.quageo.2009.02.013.SunYJLaiZPLongHLiuXJandFanQS2010Quartz OSL dating of archaeological sites in Xiao Qaidam Lake of the NE Qinghai-Tibetan Plateau and its implications for palaeoenvironmental-changesQuaternary Geochronology5236036410.1016/j.quageo.2009.02.013Open DOISearch in Google Scholar

Thiel C, Buylaert JP, Murray AS and Tsukamoto S, 2011. On the applicability of post-IR IRSL dating to Japanese loess. Geochronometria 38(4): 369–378, DOI 10.2478/s13386-011-0043-4.ThielCBuylaertJPMurrayASandTsukamotoS2011On the applicability of post-IR IRSL dating to Japanese loessGeochronometria38436937810.2478/s13386-011-0043-4Open DOISearch in Google Scholar

Thomsen KJ, Murray AS and Jain M, 2011. Stability of IRSL signals from sedimentary K-feldspar samples. Geochronometria 38(1): 1–13, DOI 10.2478/s13386-011-0003-z.ThomsenKJMurrayASandJainM2011Stability of IRSL signals from sedimentary K-feldspar samplesGeochronometria38111310.2478/s13386-011-0003-zOpen DOISearch in Google Scholar

Thomsen KJ, Murray AS, Jain M and Bøtter-Jensen L, 2008. Laboratory fading rates of various luminescence signals from feldspar-rich sediment extracts. Radiation Measurements 43(9): 1474–1486, DOI 10.1016/j.radmeas.2008.06.002.ThomsenKJMurrayASJainMandBøtter-JensenL2008Laboratory fading rates of various luminescence signals from feldspar-rich sediment extractsRadiation Measurements4391474148610.1016/j.radmeas.2008.06.002Open DOISearch in Google Scholar

Wang J, Xiao L, Reiss D, Hiesinger H, Huang J, Xu Y, Zhao JN, Xiao ZY and Komatsu G, 2018. Geological Features and Evolution of Yardangs in the Qaidam Basin, Tibetan Plateau (NW China): A Terrestrial Analogue for Mars. Journal of Geophysical Research: Planets 123: 2336–2364, DOI 10.1029/2018JE005719.WangJXiaoLReissDHiesingerHHuangJXuYZhaoJNXiaoZYandKomatsuG2018Geological Features and Evolution of Yardangs in the Qaidam Basin, Tibetan Plateau (NW China): A Terrestrial Analogue for MarsJournal of Geophysical Research: Planets1232336236410.1029/2018JE005719Open DOISearch in Google Scholar

Wu L, Prush V, Lin X, Xiao A, Zhang L, Chen N, Yang R and Chen H, 2019. Quantifying wind erosion during the late Quaternary in the Qaidam Basin, Central Asia. Geophysic Research Letters 46(12): 6378–6387, DOI 10.1029/2019GL082992.WuLPrushVLinXXiaoAZhangLChenNYangRandChenH2019Quantifying wind erosion during the late Quaternary in the Qaidam Basin, Central AsiaGeophysic Research Letters46126378638710.1029/2019GL082992Open DOISearch in Google Scholar

Xiao L, Wang J, Dang YN, Cheng ZY, Huang T, Zhao JN, Xu Y, Huang J, Xiao ZY and Komatsu G, 2017. A new terrestrial analogue site for Mars research: The Qaidam Basin, Tibetan Plateau (NW China). Earth-Science Reviews 164: 84–101, DOI 10.1016/j.earscirev.2016.11.003.XiaoLWangJDangYNChengZYHuangTZhaoJNXuYHuangJXiaoZYandKomatsuG2017A new terrestrial analogue site for Mars research: The Qaidam Basin, Tibetan Plateau (NW China)Earth-Science Reviews1648410110.1016/j.earscirev.2016.11.003Open DOISearch in Google Scholar

Yu LP, An P and Lai ZP, 2016. Different Implications of OSL and radiocarbon ages in archaeological sites in the Qaidam Basin, Qinghai-Tibet Plateau. Geochronometria (43): 188–200, DOI 10.1515/geochr-2015-0048.YuLPAnPandLaiZP2016Different Implications of OSL and radiocarbon ages in archaeological sites in the Qaidam Basin, Qinghai-Tibet PlateauGeochronometria4318820010.1515/geochr-2015-0048Open DOISearch in Google Scholar

Yu LP, Dong ZB, Lai ZP, Qian GQ and Pan T, 2015a. Origin and lateral migration of linear dunes in the Qaidam Basin of NW China revealed by dune sediments, internal structures, and optically stimulated luminescence ages, with implications for linear dunes on Titan: Comment and Discussion. Geological Society of America Bulletin 127 (1–2): 316–320, DOI 10.1130/B31041.1.YuLPDongZBLaiZPQianGQandPanT2015aOrigin and lateral migration of linear dunes in the Qaidam Basin of NW China revealed by dune sediments, internal structures, and optically stimulated luminescence ages, with implications for linear dunes on Titan: Comment and DiscussionGeological Society of America Bulletin1271–231632010.1130/B31041.1Open DOISearch in Google Scholar

Yu LP and Lai ZP, 2012. OSL chronology and palaeoclimatic implications of aeolian sediments in the eastern Qaidam Basin of the northeastern Qinghai-Tibetan Plateau. Palaeogeography, Palaeoclimatology, Palaeoecology 337–338: 120–129, DOI 10.1016/j.palaeo.2012.04.004.YuLPandLaiZP2012OSL chronology and palaeoclimatic implications of aeolian sediments in the eastern Qaidam Basin of the northeastern Qinghai-Tibetan PlateauPalaeogeography, Palaeoclimatology, Palaeoecology337–33812012910.1016/j.palaeo.2012.04.004Open DOISearch in Google Scholar

Yu LP and Lai ZP, 2014. Holocene climate change inferred from stratigraphy and OSL chronology of aeolian sediments in the Qaidam Basin, northeastern Qinghai–Tibetan Plateau. Quaternary Research 81(3): 488–499, DOI 10.1016/j.yqres.2013.09.006.YuLPandLaiZP2014Holocene climate change inferred from stratigraphy and OSL chronology of aeolian sediments in the Qaidam Basin, northeastern Qinghai–Tibetan PlateauQuaternary Research81348849910.1016/j.yqres.2013.09.006Open DOISearch in Google Scholar

Yu LP, Lai ZP and An P, 2013. OSL chronology and paleoclimatic implications of paleodunes in the middle and southwestern Qaidam Basin, Qinghai-Tibetan Plateau. Sciences in Cold and Arid Regions 5(2): 211–219, DOI 10.3724/SP.J.1226.2013.00211.YuLPLaiZPandAnP2013OSL chronology and paleoclimatic implications of paleodunes in the middle and southwestern Qaidam Basin, Qinghai-Tibetan PlateauSciences in Cold and Arid Regions5221121910.3724/SP.J.1226.2013.00211Open DOISearch in Google Scholar

Yu LP, Lai ZP, An P, Pan T and Chang QF, 2015b. Aeolian sediments evolution controlled by fluvial processes, climate change and human activities since LGM in the Qaidam Basin, Qinghai-Tibetan Plateau. Quaternary International 372: 23–32, DOI 10.1016/j.quaint.2014.09.043.YuLPLaiZPAnPPanTandChangQF2015bAeolian sediments evolution controlled by fluvial processes, climate change and human activities since LGM in the Qaidam Basin, Qinghai-Tibetan PlateauQuaternary International372233210.1016/j.quaint.2014.09.043Open DOISearch in Google Scholar

Yu LP, Roskin J and Greenbaum N, 2019. Aeolian-Fluvial Interactions Stabilize Desert in the Qaidam Basin, Qinghai-Tibetan Plateau. Geophysical Research Abstracts 21, EGU2019-19084.YuLPRoskinJandGreenbaumN2019Aeolian-Fluvial Interactions Stabilize Desert in the Qaidam Basin, Qinghai-Tibetan PlateauGeophysical Research Abstracts21EGU201919084Search in Google Scholar

Yu SS, Tan HB, Liu XQ, Cao GC, 2009. Study on Sustainable Utilization of Resources in Qarhan Salt Lake. Science Press: Beijing (in Chinese).YuSSTanHBLiuXQCaoGC2009Study on Sustainable Utilization of Resources in Qarhan Salt LakeScience PressBeijing(in Chinese)Search in Google Scholar

Yu SY, Colman SM and Lai ZP, 2018. Late-Quaternary history of ‘great lakes’ on the Tibetan Plateau and palaeoclimatic implications – A review. Boreas 48(1): 1–19, DOI 10.1111/bor.12349.YuSYColmanSMandLaiZP2018Late-Quaternary history of ‘great lakes’ on the Tibetan Plateau and palaeoclimatic implications – A reviewBoreas48111910.1111/bor.12349Open DOISearch in Google Scholar

Zhang HC, Fan HF, Chang FQ, Zhang WX, Lei GL, Yang MS, Lei YB and Yang LQ, 2008. AMS Dating on the Shell Bar Section from Qaidam Basin, NE Tibetan Plateau, China. Radiocarbon 50(2): 255–265, DOI 10.1017/S0033822200033555.ZhangHCFanHFChangFQZhangWXLeiGLYangMSLeiYBandYangLQ2008AMS Dating on the Shell Bar Section from Qaidam Basin, NE Tibetan Plateau, ChinaRadiocarbon50225526510.1017/S0033822200033555Open DOISearch in Google Scholar

Zheng D and Zhao D, 2017. Characteristics of natural environment of the Tibetan Plateau. Science & Technology Review 35(6): 13–22 (in Chinese with English abstract).ZhengDandZhaoD2017Characteristics of natural environment of the Tibetan PlateauScience & Technology Review3561322(in Chinese with English abstract)Search in Google Scholar

Zhang ZF, Zhang HP and Ma XP, 2014. Change features of average wind speed and strong wind days in Chaidamu Basin. Journal of Arid Land Resources and Environment 28(10): 90–94, DOI 10.13448/j.cnki.jalre.2014.10.015 (in Chinese with English abstract).ZhangZFZhangHPandMaXP2014Change features of average wind speed and strong wind days in Chaidamu BasinJournal of Arid Land Resources and Environment2810909410.13448/j.cnki.jalre.2014.10.015(in Chinese with English abstract)Open DOISearch in Google Scholar

Recommended articles from Trend MD

Plan your remote conference with Sciendo