Dalangtan Saline Playa in a Hyperarid Region on Tibet Plateau: I. Evolution and Environments

Abstract

Since 2008, we have been studying a saline lake, Dalangtan (DLT) Playa, and its surroundings in a hyperarid region of the Qaidam Basin on the Tibetan Plateau as a potential Mars analog site. We describe the evolution of saline deposits in the Qaidam Basin (including DLT), based on investigative findings accumulated over the course of 60 years of geological surveys. In addition, we report regional meteorological patterns recorded for the past 32 years along with meteorological station recorded data at DLT since 2012. Overall, the DLT area on the Tibetan Plateau has low atmospheric pressure, high ultraviolet radiation, low annual mean temperatures (T) but large seasonal and diurnal T cycles, and extremely low relative humidity, all of which bear some similarities with the equatorial region on Mars. In addition, salt types similar to those found on Mars, such as magnesium-sulfates, chlorides, and perchlorates, are found at the surface and subsurface in the DLT area (and the other two playas in the Qaidam Basin), thus supporting DLT as a Mars analog in terms of mineralogy and geochemistry.

1. Introduction

Studies of terrestrial analog sites have played an essential role in understanding observations from past missions. Although no site on Earth is a perfect analog to specific regions on Mars, individual analog sites on Earth do provide important scientific results that support fundamental science as applied to Mars and Mars missions.

Since 2008, our team has been studying the saline lake, Dalangtan (DLT) Playa, and its surroundings in the hyperarid region (Qaidam Basin) on the Tibetan Plateau in China as a potential Mars analog site (Kong et al., 2009, 2010; Mayer et al., 2009; Sobron et al., 2009; Wang and Zheng, 2009, 2011; Zheng et al., 2009; Wang et al., 2010, 2013; Anglés and Li, 2017a, 2017b; Cheng et al. 2017; Xiao et al., 2017). This article describes the evolution of saline deposits in the Qaidam Basin, based on the knowledge accumulated through 60 years of geological survey and detailed ground investigations (e.g., Zhang, 1987; Zhu et al., 1994; Zheng, 1997; Kong et al., 2014a, 2014b). In addition, we report on regional meteorological patterns averaged for the past 32 years. This is one of three articles based on our investigations of the DLT saline playa. In the second article, we report the analysis of the collected subsurface samples from two vertical stratigraphic cross sections at the DLT Playa, with an emphasis on mineralogy and geochemistry (Wang et al., 2018). In the third article of this series (Sobron et al., 2018), we report a multiscale mineralogy and geochemistry study of surface salts in an anticline in DLT (site 02).

This article discusses the salt precipitation history (through the Paleocene and to Pleistocene period) and distribution at different playas in Qaidam Basin along with the regional climate pattern. We note observed climatic, mineralogical, and geochemical similarities between the basin and some salt-rich areas on Mars.

2. Evolution of Saline Playas in Qaidam Basin

The Qaidam Basin is located in the northeast region of the Qinghai-Tibet (QT) Plateau. The QT Plateau has an average elevation of 4500 m and comprises five massive mountain chains that are east-west oriented and includes the Himalaya mountain chain (the highest among the five, average elevation of ∼6100 m) to the south. This setting blocks the humid Indian monsoon to Qaidam Basin, which has the lowest average elevation (2676 m, the Senie Lake) on the QT Plateau. The Qaidam Basin is thus one of the driest places in nonpolar regions on Earth, with an aridity index (AI) of 0.008–0.04 recorded at specific locations (Zhu et al., 1994).

The Qaidam Basin is surrounded by the Qilian Mountains in the northeast, the Aljin Mountains in the northwest, and the Kunlun Mountains in the south (Fig. 1). This basin terrain began to subside, due to the opposite strike-slip of three deep faults that extend along each of the three mountain ranges, and then form the primary phase of the Qaidam sedimentary basin during the Mesozoic. The high elevation of the Qaidam Basin (2700–3300 m) results in low mean annual temperatures (T), large diurnal and seasonal T variations, and high ultraviolet radiation. These environmental conditions, in addition to hyperaridity, cause the evaporation of water bodies in the Qaidam Basin and the precipitation of various salts. The Qaidam Basin features four major saline playas that formed from brine evaporation in its internal depressions.

FIG. 1.

Schematic map of Qaidam Basin.

The landforms of the Qaidam Basin have evolved since its formation. Since the Paleocene, starting with the collision between the Eurasia and India plates, the Qaidam Basin has experienced periods of subsidence, and a thick layer of sediments (up to 2600 m) has formed in the basin. In addition, regional tectonic activity, especially the uplift of the Tibetan Plateau, together with the deposition process itself, has altered the location of the depositional center several times within the basin.

The bases of the Qaidam Basin are thrust faults and strike slip faults, with main continental deposits in Mesozoic and Cenozoic. Triassic strata are absent over the basin, and deposits in Mesozoic, Jurassic, and Cretaceous are distributed in the northern margin of the basin. Jurassic strata is a set of river and lake facies, and coal-bearing swamp facies sediments with a thickness of 500 m, which indicates that the northern part of the Qaidam Basin was a freshwater lake in that time, with T consistent with a humid, subtropical climate. In the Cretaceous, a set of continental red clastic rock series developed that are mainly distributed in the northern margin of the basin. The sedimentary range was much more extensive than before. With the climate beginning to dry and water bodies changing from deep to shallow, the Qaidam Basin was essentially a collection of alluvial plains and shallow lakes.

The Cenozoic sedimentary strata developed most extensively in the Qaidam Basin and covered the whole basin. In addition, the main sedimentary formation from the Paleogene to the Neogene has been found in the western depression with a thickness of 1252–10,546 m. Sedimentary processes occurred from the upper Paleocene to the Pliocene, but the Quaternary sedimentary materials are located primarily in the eastern part of the basin. From the beginning of the early Pleistocene, a large number of salt deposits formed, most of them of 2000–3400 m thickness. Deposition occurred from the upper Paleocene to Pliocene, and gypsum salt sedimentation started to occur in the Oligocene; salt deposition was most prevalent during the Miocene.

In summary, the climate of the basin since the Cenozoic has become increasingly dry. Owing to the collision of the India plate and the Asian plate, the sedimentary center of the lake in the Qaidam Basin has migrated from the northwest to the east. By the late Pliocene, the center shifted from the northwest to the east of the basin, where the DLT Playa formed.

The Qaidam Basin is a closed drainage basin. River systems are mainly recharged by snowmelt from the surrounding mountains, whereas spring waters from deep faults and meteoritic water supply the modern lakes in the interior. Surface water bodies react with atmospheric water and with previously deposited salt-rich sediments, becoming salt ion rich. Therefore, the water chemistry of modern salt lakes in the Qaidam Basin is greatly controlled by the nature of local salt sediments. The long and complex history of salt deposits in the Qaidam Basin, especially the migration of the salt depositional center with time, has generated three major playas with different salt types: Mg-sulfate-rich DLT, chloride-rich Qarhan, and sulfate–chloride-rich Kunteyi.

2.1. Sulfate-rich sediments at the DLT Playa

As discussed previously, sulfate-rich sediments dominated during the first major salt forming period in the Pliocene and are distributed widely in the west and northwest parts of the Qaidam Basin. During this period, the sulfate-rich sediments first deposited at areas centered at the DLT secondary basin (aka DLT area, 38°0′–38°40′N, 91°10′–92°10′E), then extended to the northwest Qaidam Basin. In the late Pliocene, only a small amount of high-salinity sulfate brine was left in local depressions including the DLT depression, which eventually dried up during the Holocene to form the DLT Playa.

The DLT Playa is located in the center depression of the DLT area on the west margin of Qaidam Basin. The mineralogy of surface and shallow subsurface strata has been described in several studies (Zheng, 1997, 2009; Wang et al., 2018). The predominant sulfate phase in the strata at the edge of the DLT area is mirabilite, a hydrated sodium sulfate, Na₂SO₄·10H₂O. The strata at the center of the DLT Playa are composed mostly of hexahydrite, a hydrated magnesium sulfate, MgSO₄·6H₂O. Bloedite, Na₂Mg(SO₄)₂·4H₂O, was also identified in the DLT area (Table 1). This deposition trend from Na sulfate to Mg sulfate follows the normal geochemical evolution trend and the precipitation sequence of sulfate brines. The common occurrence of halite at the surface of the DLT and in samples collected from shallow subsurface strata at various locations of the playa supports the notion that the residual sulfate-rich brine from the first major salt forming period in the Pliocene reached the stage of halite saturation. In addition, ClO₄ ⁻ and ClO₃ ⁻ were detected in shallow subsurface regolith of the DLT Playa (Wang et al., 2018, this volume).

Table 1.

Salt Minerals Found in Three Saline Playas in Qaidam Basin and in Mars

Minerals	Chemistry	DLT Playa	Kunteyi Playa	Qarhan Playa	Mars
Gypsum	CaSO₄·2H₂O	Yes	Yes	Yes	Yes
Bassanite	CaSO₄·1/2H₂O	Yes	Yes
Anhydrite	CaSO₄	Yes		Yes
Mirabilite	Na₂SO₄·10H₂O	Yes	Yes
Thenardite	Na₂SO₄	Yes	Yes
Epsomite	MgSO₄·7H₂O	Yes
Hexahydrite	MgSO₄·6H₂O	Yes	Yes
Pentahydrite	MgSO₄·5H₂O	Yes
Starkeyite	MgSO₄·4H₂O	Yes	Yes		Yes
Kieserite	MgSO₄·H₂O	Yes			Yes
Bloedite	Na₂Mg(SO₄)₂·4H₂O	Yes	Yes
Glauberite	Na₂Ca(SO₄)₂	Yes	Yes
Glaserite	K₃Na(SO₄)₂	Yes
Leonite	K₂Mg(SO₄)₂·4H₂O	Yes
Langbeinite	K₂Mg₂(SO₄)₃	Yes
Loeweite	Na₁₂Mg₇(SO₄)₁₃·15H₂O	Yes	Yes
Polyhalite	K₂MgCa(SO₄)₃·2H₂O	Yes	Yes
Picromerite	K₂Mg(SO₄)₂·6H₂O	Yes
Halite	NaCl	Yes	Yes	Yes	Yes
Sylvite	KCl	Yes	Yes	Yes	Yes
Carnallite	KMgCl₃·6H₂O	Yes		Yes
Bischofite	MgCl₂·6H₂O		Yes	Yes	Yes
Antarcticite	CaCl₂·6H₂O		Yes
Dansite	Na₂₁Mg(SO₄)₁₀Cl₃	Yes

Adapted from Zhu et al. (1994), Mohlmann et al. (2011), Kong et al. (2014b), and Wang et al. (2018).

DLT, Dalangtan.

2.2. Chloride-rich sediments at Qarhan Playa

In the second major salt forming period of Qaidam Basin during the Pleistocene, chloride-rich sediments deposited at regions centered at the Qarhan lake area (Fig. 1). The chlorine-rich brine originated by way of migration from the west Qaidam Basin into the Qarhan depression, which eventually evaporated and formed the Qarhan Playa. Qarhan Playa is a large dry area in the Qarhan lake region (36°37′–37°12′N, 93°42′–96°14′E) at the center of the Qaidam Basin. Chloride-rich minerals, mainly halite NaCl, have been observed in the strata formed in the Pleistocene. Carnallite KMgCl₃·6H₂O, sylvite KCl, and bischofite MgCl₂·6H₂O started to form in strata from the Holocene (Table 1), representing the very late evaporation stage of chlorine-rich brine.

2.3. Deposition transition from sulfates to chlorides at Kunteyi Playa

During the first major salt deposition period in the Pliocene, the deposition center of Qaidam Basin moved to the northwest, and the sulfate–chloride-bearing brine extended to the Kunteyi saline lake area (upper–middle in Fig. 1). As this migration went on, the brine chemistry evolved to an intermediate stage, transitioning from sulfate rich to chloride rich. Subsequently, these brines partially evaporated and formed the Kunteyi Playa and the Kunteyi Salt Lake.

The Kunteyi Playa has salt-bearing strata up to hundreds of meters thick. In this region, sulfates such as gypsum CaSO₄·2H₂O, mirabilite, and glauberite Na₂Ca(SO₄)₂ occur in the lower part of the strata, whereas hydrated chlorides, for example, bischofite MgCl₂·6H₂O and antarcticite CaCl₂·6H₂O, occur in the upper part of the strata or the surface of outcrops (Table 1).

3. Regional Meteorological Patterns

3.1. Three data sets

In this work, we use three data sets to describe the meteorological patterns of the DLT area. The first set is a 32-year record (1980–2011) of meteorology data collected at the Mangya meteorological station, located <50 km from the DLT Playa (Fig. 1). Meteorological data were provided by the Qinghai Meteorological Administration. This data set includes T, relative humidity (RH), atmospheric pressure at the surface, precipitation, evaporation, wind speed, and sunlight hours. These data were recorded each hour. The second set is a 2-year RH and T record collected by our team with a data logger RHT10 (Extech Co., Nashua, NH) at the surface of the Xiao Liang Shan anticline (6 km to the center of the DLT Playa) since 2010. These data were recorded each hour and were downloaded every 3–6 months. The third set is from a new meteorological station set up by us at the center of the DLT Playa in 2012, from which the data have been collected to the present and recorded each hour. All three playas in the Qaidam Basin, as discussed in Section 2, formed at local depressions and have quite similar elevations: 2690 m, 2670 m, and 2730 m for the DLT, Qarhan, and Kunteyi, respectively. Owing to their proximity and similar elevation, the three regions are subject to the same meteorological conditions. Although our data were only collected at, or near, the DLT Playa, the DLT measurements can be extrapolated to the other two playas.

3.2. Basic environmental characteristics

Figures 2, 4, 7 –11 show the monthly average T (in °C), RH (in %), lighting (in hours), wind speed (in m/s), precipitation (in mm), and evaporation (in mm) recorded at Mangya meteorological station (<50 km to DLT Playa). Figures 3 and 5 show hourly variations of T and RH in two typical summer and winter days at logger RHT10.

FIG. 2.

Patterns of T (in °C, monthly averaged) in 1980–2011, recorded at Mangya Meteorological Station (<50 km to DLT Playa). DLT, Dalangtan; T, temperature.

FIG. 3.

Diurnal temperature variations during a typical summer month and a winter month recorded at the surface of XLS anticline from T to RH logger data (<6 km to the center of DLT Playa). RH, relative humidity; XLS, Xiao Liang Shan.

FIG. 4.

Patterns of RH (%, monthly averaged) during 1980–2011, recorded at Mangya Meteorological Station (<50 km to DLT Playa).

FIG. 5.

Diurnal variations in RH during a typical spring month and a winter month recorded at the surface of XLS anticline from T to RH logger data (<6 km to the center of DLT Playa).

FIG. 6.

Water vapor pressures variation at per hour density in 2011.

FIG. 7.

Lighting hours (monthly average) during 1989–2011 recorded at Mangya Meteorological Station (<50 km to DLT Playa).

Based on those data, we found that the annual average T in the DLT area is 3.5°C. The seasonal variation ΔT_ave is >30°C (Fig. 2), but seasonal ΔT_peak is >55°C (Fig. 3). The maximum monthly average air T was 16°C in July, with T_max >30°C occurring in the summer afternoon (Fig. 3). The minimum monthly average air T was −10.7°C in January, with T_min < −25°C occurring in the winter early morning (Fig. 3). The diurnal T variation in summer is about 20°C, and that value decreases in winter to about 15°C (Fig. 3). The atmospheric pressure at the surface of the DLT area is about 70% of atmospheric pressure at sea level. The annual average surface pressure recorded is 709 mbar (Fig. 11). The surface pressure (717 mbar) in autumn is slightly higher than that in spring (706 mbar).

RH is dependent on T and the partial pressure of water P_H2O. The DLT area is extremely dry in spring and fall, but less dry in winter and summer when monthly averaged RH can rise to >35%, although it never exceeds 40% (Fig. 4). The lowest RH values (<10%) were observed in early afternoon, with a variation of 15% between months (Fig. 5). The highest RH values (>60%) were observed in early morning, with a larger variation ∼40% between months (Fig. 5). No RH value of 100% was found among our 2 years of recorded data (2010–2011) using an RHT10 logger, which is consistent with the lack of rain in our recording interval.

The changing pattern of water vapor pressures (P_H2O) in 2011 is shown in Figure 6. Data were recorded with the logger RHT10, and P_H2O was calculated based on reference data of saturated water/ice vapor pressures (Haar et al., 1984; Wagner et al., 1994). The results indicate that the water vapor input is stronger from June to August. Water vapor transported from the west is the basic water vapor source of the DLT area. West wind fluctuations have a direct effect on the interannual change of the water vapor transport flux divergence over most of Northwest China (Wang et al., 2005). The Indian monsoon affects the southern and eastern parts of Northwest China by the southwest water vapor transport stream (Wang et al., 2005). For the Qaidam Basin, the vapor resources may have the same mechanism according to our observations.

The weather in the DLT Playa is sunny and windy. The monthly average hours of sunlight range from 220 during winter to 320 during summer (Fig. 7). The maximum monthly average wind speed occurs during spring (up to 3.5 m/s), and the minimum (about 1.5 m/s) occurs during winter (Fig. 8). The maximum wind speed can sometimes reach 20–22 m/s. A value of 20 m/s was recorded at the DLT Playa weather station.

FIG. 8.

Wind speed (monthly average) during 1989–2011 recorded at Mangya Meteorological Station (<50 km to DLT Playa).

Rainfall events in the DLT area are shown in Table 2. The annual total precipitation averaged for 32 years (1980–2011) is about 50 mm. Figure 9 shows that most precipitation (maximum <25 mm monthly average) happens in the summer months. In contrast, the evaporation rate of this region is extremely high. The strong wind, solar irradiation, and lack of vegetation all lead to an annual total evaporation of 2590 mm as averaged for 32 years. Figure 10 shows that the strongest evaporation (maximum ∼440 mm per month) occurs in the high T summer months. The AI of the DLT area, as defined by the annual total precipitation over annual total evaporation, is about 0.02 (variation over month is 0.01–0.05; Figs. 9 and 10), which classifies the DLT area as a hyperarid region on Earth.

FIG. 9.

Precipitation (monthly average) during 1989–2011 recorded at Mangya Meteorological Station (<50 km to DLT Playa).

FIG. 10.

Evaporation (monthly average) during 1989–2011 recorded at Mangya Meteorological Station (<50 km to DLT Playa).

FIG. 11.

Atmospheric pressure at surface (monthly average) during 1989–2011 recorded at Mangya Meteorological Station (<50 km to DLT Playa).

Table 2.

Measured Precipitation (in mm) from 1980 to 2011 at the Mangya Meteorological Station, Located <50 km from the Dalangtan Playa

Year	January	February	March	April	May	June	July	August	September	October	November	December	Total
1980	0.8	0.7	0.0	0.8	0.2	5.5	6.6	16.2	0.6	0.0	0.0	0.3	31.7
1981	0.0	1.1	0.0	2.9	1.0	8.8	17.8	26.2	0.9	0.5	0.0	0.1	59.3
1982	0.1	1.0	2.0	3.1	18.7	35.6	7.4	5.5	5.2	0.1	0.0	1.1	79.8
1983	0.5	0.4	1.1	0.0	2.2	16.7	28.7	6.3	2.2	2.1	0.0	0.0	60.2
1984	1.3	2.1	2.4	4.2	5.3	16.4	9.3	6.3	3.3	0.0	0.0	0.1	50.7
1985	0.2	0.0	0.3	0.0	7.8	8.5	6.8	0.7	2.4	0.0	0.1	1.9	28.7
1986	0.4	0.6	0.7	0.6	34.7	54.1	4.9	8.4	0.0	0.1	1.2	0.2	105.9
1987	0.0	0.2	1.4	5.7	5.3	24.0	9.9	0.7	1.7	2.9	0.3	0.3	52.4
1988	0.0	0.3	0.7	0.3	18.7	11.4	8.4	7.0	5.2	0.0	0.0	0.0	52.0
1989	4.6	0.0	0.8	4.8	1.5	32.9	5.3	6.8	4.0	0.5	0.0	0.5	61.7
1990	0.0	0.0	3.1	0.6	0.5	22.6	11.2	4.6	0.0	0.0	0.0	1.1	43.7
1991	0.0	0.0	0.9	4.9	0.8	3.8	7.1	14.7	0.0	0.0	0.0	0.0	32.2
1992	0.2	0.2	0.7	0.0	4.3	2.8	27.6	0.5	0.1	2.0	0.0	0.2	38.6
1993	0.6	0.9	1.6	0.0	1.8	45.0	27.1	8.9	0.0	0.0	0.0	1.1	87.0
1994	0.0	0.3	0.0	0.0	0.2	4.6	12.4	4.0	0.0	0.8	0.0	0.0	22.3
1995	0.1	1.0	0.0	5.2	0.0	4.1	2.1	3.6	12.0	4.7	0.0	0.0	32.8
1996	0.0	0.0	2.0	0.8	7.7	7.3	29.1	13.0	0.8	0.4	0.0	0.0	61.1
1997	0.0	0.0	0.0	0.0	11.0	8.8	8.3	18.2	0.0	0.0	0.0	0.0	46.3
1998	0.2	0.0	4.7	0.0	0.6	13.7	11.9	11.2	4.7	0.2	0.0	0.0	47.2
1999	0.0	0.0	2.4	0.0	0.3	19.0	13.2	4.9	0.0	0.2	0.0	0.0	40.0
2000	1.9	0.5	0.0	0.2	1.6	16.4	12.5	7.2	4.9	0.0	0.0	0.0	45.2
2001	0.0	0.4	0.0	0.0	0.8	3.9	1.1	5.8	0.1	0.0	0.0	0.0	12.1
2002	2.6	0.0	0.1	7.1	0.6	13.8	7.0	2.7	6.6	0.3	0.0	0.8	41.6
2003	0.0	1.4	3.1	0.9	4.1	21.0	14.7	0.0	2.6	0.3	0.0	0.2	48.3
2004	0.7	0.0	0.1	0.7	1.6	6.7	1.6	5.2	0.0	0.0	0.1	0.1	16.8
2005	0.0	2.2	5.4	0.0	32.4	2.6	22.5	21.3	0.6	1.3	0.0	0.0	88.3
2006	1.6	0.8	0.0	4.1	6.0	2.0	12.0	3.0	4.2	0.3	0.0	2.4	36.4
2007	0.0	0.0	0.1	0.9	2.7	17.8	14.6	0.3	11.9	1.8	0.0	0.0	50.1
2008	5.8	0.0	0.2	0.0	12.6	8.7	20.7	4.1	24.8	1.9	0.0	0.2	79.0
2009	0.0	1.2	0.3	0.0	7.7	1.0	6.3	0.0	0.2	0.0	0.0	1.1	17.8
2010	0	4.1	2.5	3.1	4.7	10.5	42.1	5.3	22.7	0.9	0	0.4	96.3
2011	0	0	0.8	2	2	12.6	6.3	15.5	3.9	0.1	0.8	0	44.0

4. DLT May Provide Some Interesting Case Studies for Mars Potential Habitability

On the basis of the already reported occurrence of salt deposits in the three playas of Qaidam Basin (including the DLT Playa), and the regional meteorological patterns, we believe that the DLT area and the local region in general can serve as a Mars analog site that is consistent with desert-type terrain and applicable for investigation of the fundamental properties of hydrous salts in a natural setting under Mars-relevant environmental conditions, such as the precipitation of salts from a natural Na-K-Ca-Mg-Cl-SO₄-CO₃-H₂O system and their phase transformation or preservation under hyperarid conditions. Because similar types of hydrous salt deposits (magnesium-sulfates) at the surface of DLT were identified on Mars, the DLT area can also serve as an orbital remote sensing test region for the use of Vis-NIR spectroscopy, with known ground truth, and for the Operation Readiness Test of future landed missions to Mars (e.g., China's Mars 2020 mission).

The diverse salts with different chaotropic or kosmotropic properties in the Qaidam Basin (especially MgCl₂·6H₂O and CaCl₂·6H₂O in the Kunteyi Playa) may provide some interesting case studies for Mars regarding potential habitability.

T and water activity are the most important physical parameters that influence microbial metabolism and growth (Beaty et al., 2006). A limit of T ≥ −25°C and water activity >0.5 has been recommended for considering Special Regions on Mars (Kminek et al., 2010). Future field exploration of the DLT region would enable detailed study of these parameters along with biomarker identification within salt deposits on-site and in laboratory study.

Footnotes

Acknowledgments

The authors thank Dr. Weigang Kong and Academician Wenjin Zhao for their help in preparing this article. This research was funded by the China Geological Survey program “Astrobiology on Mars analogous sites for saline environments” (Grant No. 12120113019100) and “The comprehensive survey of lithium, and other resources in salt lakes on the Tibetan Plateau” (Grant Nos. 121201103000150012 and DD20160025). A.W. and P.S. would like to express their great appreciation to the McDonnell Center for Space Science at Washington University in St. Louis for its generous financial support for the 2008 field expedition to Qaidam Basin, Tibetan Plateau, the laboratory sample analysis (2009–2012), and the article preparation (2014–2016).There are no competing financial interests existing for all authors of this article.

Authors' Disclosure Statement

No competing financial interests exist.

Abbreviations Used

Associate Editor: Christopher McKay

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