ORIGINAL RESEARCH article
Late Quaternary Dust, Loess and Desert Dynamics in Upwind Areas of the Chinese Loess Plateau
- 1School of Geography, South China Normal University, Guangzhou, China
- 2MOE Key Laboratory of Western China’s Environmental Systems, Lanzhou University, Lanzhou, China
- 3Department of Earth Sciences, Uppsala University, Uppsala, Sweden
As a key global climate and dust archive, the nature of Chinese loess generation, transport and deposition remains debated. The lack of consensus on dust dynamics from sources to leeward regions fundamentally limits interpretation of the preserved past climate and dust record. Here, we investigate chronostratigraphic variability of aeolian deposits in upwind regions of the modern Chinese Loess Plateau (CLP) and attempt to understand dust dynamics that potentially affects loess deposition downwind. The strata consist of alternating layers of typical loess, well-sorted sand, and sandy loess, with obvious unconformities occurring at the transitions from loess to sand. We suggest that pre-existing typical loess in regions to the northwest of the modern CLP was eroded by wind, providing a significant source of homogeneous dust for the dust deposits downwind. The sand deposits interbedded with typical loess at the study sites suggests that proximal deserts have greatly expanded and contracted repeatedly prior to the Holocene. However, the spatial extents of the deserts, as inferred from the sections here, have not markedly diminished after the major expansion during the Last Glacial Maximum. Such a pattern of proximal desert dynamics plays an important role in regulating dust emission and transport, strongly affecting dust sequences on the CLP. Our results suggest a complex scenario of dust dynamics in upwind regions of the CLP at least over the Late Quaternary; the involved processes have to be considered when using conventional proxies from Chinese loess deposits to recover the history of climate and dust changes.
As one of the world’s key climate archives, Chinese loess deposits have been widely used to decipher changes in continental environments and atmospheric circulation on various timescales (e.g., Hovan et al., 1989; Liu and Ding, 1998; Guo et al., 2002; Sun et al., 2012; Licht et al., 2014). However, the nature of loess generation and deposition and the processes that could affect these have generally not been investigated in detail within loess-based climatic reconstructions, with most studies assuming largely consistent dust emission, transport and deposition for given intervals.
Chinese loess deposits are mainly derived from the arid and semiarid regions of China, constituting source proximal dust deposits of the Asian aeolian system (Rea, 1994; Biscaye et al., 1997; Uno et al., 2009; Shao et al., 2011). Thus, loess deposition must be affected by a complex range of surface processes and local influences (Stevens et al., 2006), including aridity in source areas, dust transport capacity, and changes in the scope of source areas and hence in materials supplying dust. Kapp et al. (2015) mapped the landforms of the Ordos Basin and the northern Chinese Loess Plateau (CLP), and concluded that thick loess may have been previously distributed in areas further to the north and west than the present CLP, but was subsequently eroded by winds, supplying homogeneous dust to younger loess deposits leeward. This work emphasized that loess in upwind regions from the current CLP would be a previously unrecognized dust source, suggesting a process of “aeolian cannibalism” of previously deposited loess. A large amount of zircon U-Pb data from loess and different potential dust source deposits suggest that a substantial portion of interglacial dust is recycled from older glacial loess (Licht et al., 2016), implying reworking of older loess deposits by wind. Furthermore, multiple erosional hiatuses during the past 300 ka, recorded by loess deposits at Jingbian, provide independent evidence that supports the hypothesis of loess cannibalization from CLP marginal areas (Stevens et al., 2018). These findings therefore call for urgent reassessments of changes in potential sources of Chinese loess, of accepted interpretations of climatic proxies applied to loess deposits, such as sedimentation rate and grain size, of Quaternary dust dynamics in this globally important dust emission region, and even exactly how the Chinese loess time series can represent large-scale climatic changes. To test these findings requires analysis of the complex sedimentary system source to sink, including understudied aeolian sediment that lies between the main CLP and the main source areas. However, to date, beyond a few well dated sites (Xu et al., 2018), there is still a lack of chronostratigraphic evidence over the age and geographical extent of loess upwind of the main CLP. Potential previously active depositional regions are currently dominated by desert landscapes and subjected to intense aeolian erosion. This means the potential for pre-existing loess to act as a dust source and for the influence of proximal desert activity on loess accumulation on the CLP remains unclear.
In this study, we investigate chronostratigraphic variability and changes in grain size of aeolian deposits outside the boundary of the modern CLP, focusing on dust activity in upwind areas of the CLP and its potential impacts on loess accumulation downwind. Here, the “upwind areas” is referred to by considering the modern transition zone between proximal deserts and the loess plateau and the areas today characterized by patches of moving sand. This work aims to understand (1) the possible distribution of pre-existing loess areas in upwind regions of the CLP, (2) the influence of dust entrained from pre-existing loess on the CLP loess, and (3) the evolution of proximal deserts during the Late Quaternary and the potential impact on loess sequences. Our results provide insights into dust dynamics in regions upwind of the CLP, which are crucial for understanding environmental and climatic changes recorded by loess sequences from the CLP and in constraining the specific dust source areas of one of the most important dust source regions in the world.
Study Sites and Methods
As an intermediate product of airborne transport, aeolian deposits between proximal deserts and the CLP share features of both source materials and loess deposits (Qiang et al., 2010), and thus are a crucial link in deciphering dust dynamics between source areas to dust depositional regions. Three outcrop sections of aeolian deposits at two sites northwest of the modern CLP were selected for detailed investigation (Figures 1, 2). Two sections in the Xiangshan Mountains (sections XS-A and XS-B; 37°20′8″N, 105°13′36″E) are on a rocky platform of tectonic origin along the central northern slopes of the range, which is separated from the Tengger Desert by the Yellow River (Figures 1, 2). The site is at an altitude of 1645 m a.s.l. and is ∼500 m higher than the Yellow River. The mean annual temperature and precipitation of the area were 9.7°C and 187 mm, respectively during 1965–1980 (Qiang et al., 2010), and the maximum wind speed in spring was 29.1 m s–1. The Kajia section (KJ; 35°33′27.6″N, 100°58′44.3″E) is located at the southeastern margin of the Mugetan Sandy Land in the Gonghe Basin on the NE edge of the Qinghai-Tibetan plateau, at an altitude of 3280 m a.s.l. (Figures 1, 2). The mean annual temperature and rainfall were 2.3°C and 403 mm over the past 50 years.
Figure 1. Physical environments along the boundary between proximal deserts and the Chinese Loess Plateau (A). Locations of the studied sites and the referenced loess sites are shown by red solid squares. Close-up view (Google EarthTM) of the physical environments surrounding sections XS-A/B (B) and KJ (C).
Figure 2. Photographs of sections XS-B (A), XS-A (B), and KJ (C). Dashed lines indicate stratigraphic boundaries. Flat surfaces, clearly identified at the transitions from loess to sand deposition in the section, are characterized by abrupt alternation of sediment, no signs of fluvial activity, and inclination to the direction of prevalent winds in winter and spring seasons, indicating erosional hiatuses by wind.
Bulk samples were collected from the sections at intervals of 2–10 cm. Sediment grain-size distributions were measured using a laser particle analyzer (Malvern Mastersizer 2000), after removing organic matter and carbonate by H2O2 and HCl followed by dispersion with (NaPO3)6. The measurement range is 0.02–2000 μm.
Considering that the quartz optically stimulated luminescence (OSL) signal is likely to be saturated for pre-Late Quaternary strata, the chronologies of sections XS-B and KJ and the age of sample XS-A-07 are determined using K-feldspar post-IR Infra-Red Stimulated Luminescence (IRSL) techniques (Buylaert et al., 2012, 2015). Sample preparation followed the methods described by Aitken (1998). All laboratory processing, including sample preparation and luminescence measurements, was carried out in a darkroom under subdued red light in the Luminescence Laboratory at Lanzhou University, China. All samples were treated with 10% HCl and 20% H2O2 to remove carbonate and organic matter, respectively, and then wet sieved to extract sediments of grain sizes of 63/90–125 μm. Heavy liquid with a density of 2.58 g cm–3 was used to separate the K-feldspar fraction of each sample. The K-feldspar grains were treated with 10% HF for 40 min to remove the outer layer irradiated by alpha particles. All samples were further treated with 1 mol l–1 HCl for 10 min to remove fluorides produced during the HF etching. K-feldspar IRSL signal was measured using an automated Risø TL/OSL-DA-20 reader. Laboratory irradiation was carried out using 90Sr/90Y sources mounted within the reader. The IRSL signal was detected using a photomultiplier tube with the IRSL passing through BG-39 and Coring-759 filters. A pIRIR dating protocol, utilizing a post-IR IRSL signal stimulated at 290°C, was used for K-feldspar equivalent dose determination of coarse-grained K-feldspar (60/90–125 μm).
A prior IR stimulation temperature plateau test (Buylaert et al., 2012; Yi et al., 2016, 2018) was conducted on the sand sample XS-A-07 to check the stability of the pIRIR signal. The pIRIR De values were obtained in six groups of aliquots with different prior IR stimulation temperature from 50 to 270°C measured at 30°C intervals (three aliquots each group). The pIRIR Des have not shown an obvious trend with prior IR stimulation temperature increasing from 50 to 230°C (Figure 3), indicating the stability of pIRIR signal. A prior IR stimulation temperature of 50°C is used in pIRIR dating protocol.
A dose recovery test was conducted on sunlight bleached samples XS-B-01 (sand) and XS-A-07 (loess) to check the suitability of the chosen pIRIR dating protocol. Seven aliquots of each sample were bleached under sunlight for 28 h in March in Lanzhou, China. The residual dose of each sample was measured by using the pIRIR dating protocol and then a given dose of the 59.4 Gy was added to four bleached aliquots of sample XS-B-01 and a given dose of 297 Gy were added to four bleached aliquots of sample XS-A-07. The pIRIR De of these two samples are then measured by using the pIRIR dating protocol. The measured/given dose ratio of the K-feldspar sample XS-B-01 and XS-A-07 is 0.91 ± 0.01 and 0.89 ± 0.02, respectively. If the measured residual doses of 4.63 ± 0.13 Gy and 7.85 ± 0.40 Gy were subtracted from the corresponding measured dose, the measured/given dose ratios are 0.83 ± 0.01 and 0.86 ± 0.02. Given the uncertainty of the measurement of the residual dose, these measured/given dose ratios are considered acceptable for the pIRIR dating protocol.
The environmental dose rate was calculated from the measurements of radioactive element concentrations in the sample with a small contribution from cosmic rays. For all samples, the concentrations of uranium (U), thorium (Th), and potassium (K) were determined using neutron activation analysis (NAA). All results were converted to beta and gamma dose rates using the conversion factors by Guérin et al. (2011). The dose rate from cosmic rays was calculated from the sample burial depth and the altitude of the section (Prescott and Hutton, 1994). The internal dose rate of K-feldspar grains was calculated with a K content of 12.5% ± 0.5% (Huntley and Baril, 1997) and a Rb content of 400 ± 100 ppm (Huntley and Hancock, 2001). The measured in situ water content was used to calculate ages for all loess/sand samples. Fifty percent of individual measured value was taken as water content errors.
The stratigraphic units of the aeolian deposits are easily identified in the field and are mainly composed of loess, aeolian sand, and sandy loess/paleosol in the upper parts of the sequences (Figure 4A). Aeolian sand is homogenous and yellowish in color, with a loose structure. Loess is homogenous, finer and denser compared to the aeolian sand, and has no visible signs of pedogenic alteration. Sandy loess contains several weakly developed paleosols characterized by a massive and dense structure, abundant apertures, and secondary filamentous carbonates. These features make the paleosols more resistant to wind erosion compared to sand layers, resulting in the formation of loess/paleosol cliffs due to sand collapse (Figure 2B). In section KJ, aeolian deposition was interrupted by fluvial processes at a depth of 250 cm, producing a layer of gravels and overbank silty sand deposits (Figures 2C, 4A).
Figure 4. Stratigraphy and variations in mean grain-size (Mz) of aeolian deposits in sections XS-A, XS-B, and KJ (A). For section XS-A, changes in the sand fraction (>63 μm) are shown by a purple line. Red arrows indicate abrupt changes in Mz, representing unconformities. Photograph shows an unconformity between loess and aeolian sand. Changes in mass accumulation rate (MAR) and Mz of the Xifeng loess during the last glacial (Stevens et al., 2016) (B), which are compared with an unconformity occurring between 42.5 and 25.4 ka in section XS-A. The inconsistency between MAR and Mz from 39 to 32 ka is highlighted in darker gray.
Together with previously published quartz OSL ages (Qiang et al., 2010) and a quartz OSL age from section XS-A (sample XS-A-04) using the same methodology, 21 luminescence dates are presented here (Figure 4A and Table 1). The decay curves and growth curves for coarse-grained K-feldspar sample XS-B-02 are shown in Figure 5. The initial pIRIR290 signal shows much higher values compared to the IR50 signal. The growth curve for the sample can be readily fitted using a single saturation exponential function. The 2D0 (luminescence saturation parameter) estimated from the growth curves of pIRIR290 signal of the sample is 694 ± 37 Gy, indicating an upper limit of 700 Gy of pIRIR290 signal for samples from this region. Similarly, the pIRIR290 signal has shown a similar but slightly higher saturation dose of 800 Gy for loess samples from the Jingbian desert marginal site (Stevens et al., 2018). As a result of saturated or near saturated signals (De value exceeding c. 700 Gy, the average 2D0 value for these samples), the K-feldspar pIRIR ages from the lower parts of sections XS-B and KJ are taken as minimum age estimates (Table 1). Although we attempted to constrain the chronology of sub-strata in the lower parts of the sections, the results suggest that these deposits seem to be much older than the upper age limit of applied luminescence dating strategy. Nonetheless, the obvious changes in the nature of the deposits, as described previously, are still useful in investigating alternations of dust dynamics in the past.
The loess is dominated by silt-sized material, with modal sizes varying from 30 to 50 μm (Figure 6). In contrast, the aeolian sand has a modal size of >100 μm and contains a small amount of fine silt (<20 μm). Within sections XS-A and XS-B, the mean grain sizes (Mz) of the loess and aeolian sand fluctuate around 45 and 100 μm, respectively (Figure 4A). The Mz of the sand deposits in section KJ is slightly coarser than in sections XS-A and XS-B. This may be because the elevation of the site is similar to that of the upwind dune fields, which are relatively close to the section (Figure 1C). The Mz of sandy loess in the upper sections at these sites varies between values typical of aeolian sand and loess in the sections, reflecting mixtures of sand-sized particles and loess silts. In section XS-A, the >63 μm fraction exhibits a changing pattern very similar to that of the Mz. The sand fraction in loess accounts for around 30%, while in aeolian sand, approximating to 90%. Moderate percentages of the sand fraction (40–50%) are observed in sandy loess (Figure 4A).
Figure 6. Contrasting grain-size distributions of representative samples of loess and aeolian sand, compared with those of a sample of typical loess from Lanzhou and a sample of mobile dune. Samples depths are given in parentheses.
Potential Reworking of Pre-existing Loess in Upwind Areas
The strongly contrasting strata suggest that the deposition at the study sites was episodically dominated by distinctly different aeolian dynamics and depositional settings. The loess deposits have grain-size distributions very similar to that of a typical loess sample from Lanzhou in the western CLP (Figure 6). Given windward nature of the loci where aeolian deposits are preserved, the loess strata likely represent intervals dominated by a steppe environment, which can effectively protect deposited loess from subsequent aeolian erosion (Sun and Ding, 1998). By contrast, the aeolian sand is well-sorted, with grain-size distributions similar to that of a sand sample from mobile dunes, although the grain sizes are finer overall than the latter (Figure 6). At the XS site, sand deposition has been ascribed to the piling-up of sand due to the frequent occurrence of sand-laden storms across the adjacent deserts and to topographical effects, since in situ desertification and development of climbing dunes were ruled out (Qiang et al., 2010). Thus, compared to the interbedded loess, the sand deposits reflect either a reduced distance from sand sources to the sites and/or a strong wind regime (e.g., Ding et al., 1999); however, if so, this does not exclude the possibility that dune fields may have expanded into the vicinity of section KJ, given their similar altitude.
Abrupt increases in Mz occurred at the transitions from loess to aeolian sand, i.e., roughly varying from 45 to 100 μm (Figure 4A); whereas from aeolian sand to loess layers, the Mz decreases in a gradual manner. The abrupt grain-size changes are also clearly reflected in the distinctly different degree of compactness of loess and sand, as observed in the field. These points to sedimentation discontinuities at the loess to sand transitions. There are no signs of fluvial sediments and/or fluvial disturbance in the vicinity of the unconformities. Furthermore, the unconformity surfaces are easily identified in a large exposed area around the sampled sections (Figure 2), and are almost flat, slightly inclined to northwest (Figures 2A,B). The inclination is largely consistent with the direction of prevalent winds in seasons of intense aeolian activity in the study areas (Sun et al., 2001; Qiang et al., 2014). Thus, we argue that the abrupt changes in grain size and alteration of stratigraphic units could represent unconformities induced by aeolian erosion. There are at least four such stratigraphically identified hiatuses in the studied sections (Figure 4A). An apparent hiatus occurred from 42.5 to 25.4 ka in section XS-A, probably corresponding to one appearing at the depth of 390 cm in section XS-B, in light of an age of 14 ka from the middle of overlying sand layer. During this ∼17-ka interval, airborne material may not have settled, and/or previously deposited loess may have been partially eroded by wind. We consider that the latter is very likely, taking into account the geomorphological signs and the drastic changes in grain size at the study sites described above. The exact timings of hiatuses in the lower parts of sections XS-B and KJ cannot be constrained due to the saturated luminescence signals meaning only minimum ages can be provided, and the large uncertainties inherent in the obtained dates.
Accounting for the locations of aeolian deposits, their stratigraphic variability and the OSL/pIR IRSL dating, our results show that typical loess was previously deposited in the regions northwest to the CLP. The multiple erosional hiatuses uncovered at the transition from loess to aeolian sand here strongly suggest that considerable amounts of pre-existing loess may have been significantly and episodically eroded by wind in these areas. As such, combined with evidence from desert marginal sections to the north of the CLP (Stevens et al., 2018), our chronostratigraphic evidence from sites northwest of the CLP lends further support to a proposed “aeolian cannibalism” model of the evolution of the CLP (Kapp et al., 2015; Licht et al., 2016). Evidence from these CLP marginal areas points to previously more extensive loess cover that was subject to considerable erosion beyond the limits of the current CLP. Moreover, at section KJ, the upper loess/weak paleosol was truncated by fluvial process, and riverine deposits occurred between 19.3 and 17.4 ka. It is worthwhile noting also that besides eolain erosion, fluvial processes may have been another active agent for reworking of older loess (Licht et al., 2016). However, we note here that it is currently difficult to assess the volume of pre-existing loess in these CLP external sites that may have been removed, and therefore the degree to which these areas may once have made up an extended CLP, as envisaged by Kapp et al. (2015) and Licht et al. (2016). Nonetheless, our results show the important role that reworked loess on the margins of the CLP has in terms of dust sources to the CLP and beyond, as explored below.
The Effect of Wind Erosion of Pre-existing Loess on Dust Influx to the CLP
Dust from previously deposited loess upwind of the CLP can be entrained and then settled as components of CLP loess accumulation. However, examination of such a dynamic linkage requires a refined chronology of loess sequences. Recently, according to nine well-dated loess sections, Xu et al. (2018) suggested that there is an obvious seesaw pattern in dust accumulations during the past 20 ka across the CLP, and that the higher accumulation rates in the northwestern CLP during 20–15 ka may have been contributed to by loess reworking in upwind regions.
As for specific sites on the CLP, based on high stratigraphic resolution OSL dating, Stevens et al. (2016) measured changes in grain size and mass accumulation rate (MAR) during the last glacial at Xifeng (Figure 1 for location). This study showed that an increase in MAR between 39 and 32 ka at the section was not accompanied by an increase in grain size (Figure 4B), which is in conflict with the prevailing view that the two variables are highly correlated in loess (e.g., Vandenberghe et al., 1997). However, this contradiction and the enhanced dust MAR at Xifeng can potentially be explained by the occurrence of an erosional unconformity from 42.5 to 25.4 ka in section XS-A (Figure 4A): the increased MAR recorded at Xifeng could be a response to the deflation of pre-existing loess in upwind regions, followed by re-deposition downwind on the CLP, while the grain size was relatively invariant because the eroded and subsequently redeposited material itself consisted of loess. Indeed, our observation may explain general mismatches between grain size and dust MAR on sub-orbital timescales seen at a number of sites on the CLP (Stevens and Lu, 2009; Újvári et al., 2016). Similar unconformities in the lower parts of sections XS-B and KJ imply that wind erosion of previously deposited loess might occur within a number of intervals prior to the Late Pleistocene.
We suggest that the conversion of upwind loess deposits to dust sources must therefore be considered when using the loess deposits of the CLP to reflect large-scale patterns of Asian dust transport and deposition. For example, dust MAR estimated from loess deposits, some of which have been used to help simulate past relative dust loading (e.g., Albani et al., 2015), may be enhanced at the central CLP sites by this process, potentially leading to overestimates of dust source activity in regions further upwind of the Loess Plateau. Furthermore, the input of homogeneous, silt-sized particles of pre-existing loess from upwind areas would bias the grain size of corresponding loess deposits on the CLP to be less variable or even to be overall smaller compared to their adjacent strata, as grain size is a function not only of wind speed but also source sediment characteristics and distance to source (Újvári et al., 2016). In this case, it is unrealistic to simply explain reductions in grain size as indicating stable or weaker wind regimes, or even strengthened summer monsoonal circulation over the CLP. Rather, intensive aeolian activity may have been occurring in upwind areas at those times.
The Role of Proximal Desert Evolution on Dust Dynamics
Given that sand-sized particles are transported for short ranges even under strong wind conditions (Pye, 1987), the homogenous, well-sorted sand deposits at the study sites primarily reflect expansions of proximal deserts, e.g., the Tengger Desert and the Mugetan Sandy Land (Figure 1). As shown in section XS-A, the recent expansion of the Tengger Desert occurred during 25.4–12.2 ka, or somewhat earlier, which might be supported by the presence of sand deposition in section XS-B, dated as old as 14.0 ka (Figure 4A). Multiple episodes of expansions of proximal deserts are also indicated by the sand deposition in sections KJ and XS-B.
The grain-size variability along the profiles can further clarify the spatial variation of proximal deserts, since the advance-retreat cycles of the deserts play an important role in defining the grain size of loess deposition (Ding et al., 1999). Beneath the sandy loess/paleosol in the upper parts of the sections, the alternating loess and sand units exhibit contrasting Mz values, with relatively uniform values within their respective units (Figure 4A). In addition, in sections XS-B and KJ, the typical loess deposited above sand layers has grain-size distributions very similar to the older loess underlying the sand layers (Figures 4A, 6). These observations imply that when the typical loess is deposited at the sites, the active, previously expanded proximal deserts, represented by the layers of well-sorted sand deposition, may have greatly contracted and/or even been completely fixed following the initiation of loess accumulation. According to investigations on grain sizes of coeval loess deposits along a transection from north to south across the CLP, Ding et al. (1999) proposed that sand content (>63 μm proportion) of loess in the marginal areas of the CLP could monitor changes in the extent of proximal deserts over the past. Taking section XS-A as an example (Figure 4A), during 66.0–42.5 ka the lower sand content (<30%) of the loess suggests a possible distance of ∼100 km to the desert at that time, in light of the model proposed by Ding et al. (1999). This is much larger than the modern distance of ∼20 km (Figure 1B). Similar situations are recorded by sections KJ and XS-B, suggesting a dynamic desert environment generally. In this respect, our results are in contrast to the conclusion that the Tengger Desert has been a relatively constant active sandy desert environment since 0.68 Ma (Li et al., 2014). In fact, a paleo-megalake in the desert occurred from 42 to 18 14C ka B.P. (Zhang et al., 2002), despite the radiocarbon dates possibly being underestimated (e.g., Madsen et al., 2014). Core sediments from the Badain Jaran Desert also show that from 0.65 to 0.45 Ma a large lake occupied the desert center (Wang et al., 2015). Furthermore, episodic expansions of the Mu Us Sandy Land during the Marine Isotope Stages (MIS) 2–4 and 6 are illustrated by either erosional hiatuses or sand deposition recorded in the well-dated Jingbian section (Stevens et al., 2018). Moreover, even if we assume that the duration of the paleo-megalake in the Tengger Desert is correct, then the lake expansion seems to coincide with the erosional hiatus from 42 to 25.4 ka in section XS-A, rather than loess deposition. This would suggest that any causal links between these events are quite complicated. Although the available evidence cannot depict the detailed history of proximal deserts, it is plausible that the region may have experienced drastic hydroclimatic changes, which dramatically affect dust emission and transport, and hence the nature of aeolian deposits downwind, as observed at the study sites.
Given the intermediate Mz of sandy loess/paleosol, compared to lower loess and sand in section XS-A (Figure 4A), the Tengger Desert may not have retreated as drastically after the recent phase of expansion at 25.4–12.2 ka as occurred previously, when the typical loess units were deposited. Although the weakly developed paleosols perhaps depict a relatively warm and wet climate during some intervals of the Holocene (Figure 4A), the desert may still have had areas of activated aeolian sand sufficient for the sandy loess to be deposited throughout the Late Glacial and the Holocene. In section KJ, the sandy loess/paleosol occurred since 17.4 ka, and the Mz values are intermediate and less variable until the present. These suggest that the Mugetan Sandy Land could already have existed at this time and may even have been very close to its modern position, likely reflecting proximal desert expansion during the Last Glacial Maximum (LGM) in this area. In fact, the proximal deserts in northern China had expanded greatly during the LGM, and the Tengger Desert and the Gonghe Sandy Land areas have been estimated to be greater by ∼30 and 20% of their modern sizes, respectively (Lu et al., 2013). In addition, an observed sedimentary hiatus or erosional unconformity in sediments of an alluvial fan-lake system on the southern Alxa Plateau suggests that intense deflation occurred during the LGM (Yu et al., 2019). Intensive wind erosion also occurred in the western Alxa Plateau, as indicated by a prolonged interval of exposure and deflation of high shorelines at the eastern Juyanze paleo-lake (Li et al., 2015). Such large-scale desert expansions and wind erosion in dust source areas were probably driven by an abrupt shift to an extremely cold and dry climate during the LGM (Stevens et al., 2013).
Given a material linkage between source and sink, it is expected that this large-scale desert expansion would be tracked in loess records downwind. In fact, an increase in the accumulation rate of loess deposits downwind occurred at ∼20 ka, as evidenced by a ∼2.5-m-thick unit in the Beiguoyuan section on the northern CLP; moreover, the sediment source of this unit shifted abruptly to a local source from the previous well-mixed and recycled remote sources (Stevens et al., 2013). A high MAR of loess deposition during the LGM appears to be observed in large regions, even on the Serbian Titel Loess Plateau (Stevens et al., 2016; Perić et al., 2019). Indeed, based on closely spaced OSL dates, the loess MARs estimated at eight sites on the CLP were distinctly higher from ∼23 to 19 ka (Kang et al., 2015). Under colder and drier climatic conditions during the LGM, enhanced dune activity resulted in erosion of underlying loess strata and hence hiatuses in marginal loess sections (Stevens et al., 2013, 2018). Expanded dune fields and entrained pre-existing loess materials upwind of the CLP would have led to MAR increases together over the CLP. In this regard, the high loess MARs on the CLP during the LGM might not necessarily represent greater wind strength (e.g., Kang et al., 2015) or enhanced silt production through grain to grain impacts and abrasion in migrating dune systems (Amit et al., 2014; Lancaster, 2020), but rather erosion of pre-existing upwind loess and deflation of widespread silt deposits stored in deserts, alluvial fans and river floodplains (e.g., Derbyshire et al., 1998). However, higher wind speeds could still be one of the crucial factors for sand movement in desert environments and sand movement would still be required to erode and mobilize the silt particles locked up in loess deposits upwind of the CLP. Similarly, such a causal linkage between expansions of proximal deserts and loess deposition has to be considered for some intervals prior to the LGM, as suggested by the stratigraphically lower sand layers at the study sites, but assessment on this requires refined chronology of aeolian deposits around the CLP and desert margins.
The alternating strata of loess and well-sorted sand at the study sites show that typical loess deposits have been distributed in upwind areas of the present CLP. The pre-existing loess was eroded by winds capable of moving sands within some intervals of the Quaternary and episodically transformed to an additional dust source for loess accumulation on the CLP. The entrained loess materials will obviously result in changes in grain size and MAR of CLP loess sequences. This process provides a reasonable explanation for the recently observed contradictions between the two parameters in the late glacial loess deposits on the central CLP. Furthermore, the variable extent of proximal deserts also plays an important role in dust emission and transport, giving rise to major changes in dust accumulation rates on the CLP, especially during the LGM expansion of proximal deserts. Our results firstly provide stratigraphic evidence supporting at least some cannibalization of previously deposited loess (Kapp et al., 2015) outside of the modern CLP, and highlight dynamic dust activity in upwind regions that apparently complicate climatic interpretations from Chinese loess sequences. Despite of some dating uncertainties presented here, the significantly contrasting stratigraphic variability strongly suggests that the history of dust activity in upwind regions is of particular significance for thorough understanding of climate and dust changes recorded by Quaternary loess deposits. Thus, more well-dated aeolian sequences from broad upwind areas of the CLP, in combination with other types of environmental records, would be important to elucidate these dust processes, including changes in desert environment and their potential forcing mechanisms.
Data Availability Statement
The raw data supporting the conclusions of this article will be made available by the authors, without undue reservation.
MQ designed the work. MQ, TS, and GL wrote the text. TS, GL, and JC participated in dating analyses. LH, XW, and WL participated in the field and laboratory works. All authors read and approved the submission.
This research was supported by the National Natural Science Foundation of China (grants 42071109, 41671190) and the National Key R&D Program of China (grant 2017YFA0603402).
Conflict of Interest
The authors declare that the research was conducted in the absence of any commercial or financial relationships that could be construed as a potential conflict of interest.
We thank Hui Zhao and Shengli Yang for their assistance in luminescence dating and data analyses and Fengshan Li and Ganggang Wang for their assistance in the field.
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Keywords: dust, aeolian deposits, erosional hiatus, proximal desert, Chinese loess
Citation: Qiang M, Stevens T, Li G, Hu L, Wang X, Lang W and Chen J (2021) Late Quaternary Dust, Loess and Desert Dynamics in Upwind Areas of the Chinese Loess Plateau. Front. Earth Sci. 9:661874. doi: 10.3389/feart.2021.661874
Received: 31 January 2021; Accepted: 25 March 2021;
Published: 14 April 2021.
Edited by:Shiyong Yu, Jiangsu Normal University, China
Reviewed by:Hao Long, Nanjing Institute of Geography and Limnology (CAS), China
Zhiwei Xu, Nanjing University, China
Copyright © 2021 Qiang, Stevens, Li, Hu, Wang, Lang and Chen. This is an open-access article distributed under the terms of the Creative Commons Attribution License (CC BY). The use, distribution or reproduction in other forums is permitted, provided the original author(s) and the copyright owner(s) are credited and that the original publication in this journal is cited, in accordance with accepted academic practice. No use, distribution or reproduction is permitted which does not comply with these terms.
*Correspondence: Mingrui Qiang, email@example.com