# Whether the Middle Eocene Salt-Forming Brine in the Kuqa Basin Reached the Potash-Forming Stage: Quantitative Evidence from Halite Fluid Inclusions

Authors: Yang Xu; Yangtong Cao; Chenglin Liu
Journal: Geofluids
 (2021)

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## Abstract

The Kuqa Basin is an important potentially potash-bearing basin in China, and thick salt-bearing strata were deposited under the influence of multistage Tethyan transgression-regression cycles during the Eocene. At present, research on the process of potash formation in the Kuqa Basin has mostly focused on traditional salt mineralogy, whole-rock geochemistry, and evaporite sedimentary evolution characteristics. However, research on the original ore-forming parent fluid directly related to potash formation has not yet been carried out, directly hindering further evaluation of potash mineralization. Therefore, this paper takes the internal factors controlling potash formation as the starting point and analyzes the physical and chemical properties, such as the homogenization temperatures (Th) and chemical compositions, of primary halite fluid inclusions. A total of 220 Th data from fluid inclusions were obtained, and the temperatures ranged from 9.4 to 54.1°C, indicating a high-temperature brine environment conducive to the rapid deposition of the potash deposit. In total, 22 halite fluid inclusions were analyzed for chemical components. The highest KCl content reached 0.59%, which was higher than the lowest industrial grade of potassium-rich brine (0.5%), indicating that the brine experienced a high degree of evaporation and concentration during the salt-forming period and reached the potash precipitation stage. This paper provides quantitative data on the evolution of the sedimentary environment in the Kuqa Basin and supports future potash exploration.


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## Body

## 1. Introduction

Global evaporites were concentrated in the Tethys region during the Mesozoic and Cenozoic, and in time and space, a series of evaporites and potash deposits developed sequentially from older in the west to younger in the east [1]. Although the Kuqa Basin, located on the northern branch of the eastern section of the Tethyan region, developed thick evaporite deposits in the Cenozoic, only some potassium minerals have been discovered to date and potash deposits with industrial mining value have not been found [2–4]. Liu et al. [5] proposed that the formation of potash deposits is the result of extremes in three coupled components: “climate, tectonics, and provenance”. The Paleocene-Eocene thermal maximum (PETM) was the warmest global climate event in the Cenozoic, and this high-temperature event continued into the early Eocene, when temperatures began to slowly decrease until global warming occurred again in the middle Eocene climate optimum (MECO) [6–9]. There were favorable conditions for the formation of potash deposits in the Kuqa Basin during the Eocene, such as multistage provenance replenishment of Tethyan seawater and a relatively stable and enclosed tectonic structure [2, 10–12]. Many studies report that the Kuqa Basin has broad prospects for potash formation. However, the question of whether the Kuqa Basin reached the stage of potash precipitation currently remains controversial in the mineral deposit community. The most direct approach to answer this question is to determine the evolution stage of brine during the salt-forming period.Salt-forming brine is primary brine concentrated after the precipitation of rock salt, and it is an ore-forming fluid with a higher evaporation degree than that of rock salt. Restoring salt-forming brine evolution is a direct and reliable method to evaluate the potential for potash formation. Halite fluid inclusions are a good geological archive of brine during the salt-forming period and can provide quantitative and reliable data for studying the temperature, chemical composition, and evolution characteristics of paleobrine associated with potash mineralization. Fluid inclusions are undoubtedly an excellent geological thermometer. At present, scholars in China and other countries have conducted considerable research and widely discussed methods for measuringTh in halite fluid inclusions and its representative geological significance. Roberts and Spence [13], Lowenstein et al. [14], Zambito and Benison [15], and Zhang et al. [16] conducted research on the Th of single-phase liquid fluid inclusions in primary halite crystals made artificially in the laboratory and collected from ancient and modern salt lakes, and they showed that the measured Th quantitatively represents the brine temperature and is close to the atmospheric temperature. Moreover, a high-temperature environment is conducive to shortening the time interval from brine concentration to potash precipitation; so, high-temperature brine can be used as an important indicator of potash formation. This situation is obviously manifested in the northern Shanxi Basin, Sichuan Basin, and Lanping-Simao Basin and the Sakon Nakhon Basin in Laos [17, 18]. Single-phase fluid inclusion components can reflect chemical information during brine evolution and have been widely used in many applications, such as the study of ancient seawater or lake water chemical evolution. Lowenstein et al. [19] used the chemical compositions of halite fluid inclusions for the first time to restore the variations in Phanerozoic seawater. In addition, halite fluid inclusions have been used to study the brine evolution process in salt-forming basins [20–23].Therefore, this paper takes the internal factors controlling potash formation as the starting point and comprehensively analyzes the evolution stage of middle Eocene salt-forming brine in the Kuqa Basin by studying the evolution patterns of the temperatures and the chemical compositions of halite fluid inclusions. This paper uses halite fluid inclusions for the first time to quantitatively and directly reconstruct various ion concentrations in the middle Eocene salt-forming brine, which has great significance for potash exploration in the Kuqa Basin.


## 2. Geological Setting

The Tarim Basin experienced multiple marine transgression-regression cycles associated with the Tethys during the Late Cretaceous-Paleogene [24]. Seawater invaded the southwestern Tarim Basin through the Alay Valley in the Late Cretaceous. When the sea level rose in the early Paleocene, the Tethyan transgression range expanded and extended to the Kuqa Basin (Figure 1). At present, the timing of the final retreat of seawater from the Tarim Basin is considered to have occurred between 47 and 33 Ma [24–27]. The key factor controlling the retreat was the northward spur of the Pamirs, not the collision between India and Eurasia [28–30]. The Paleogene transgression-regression cycles in the Kuqa Basin were intermittent, and during each regression, sedimentation in the basin gradually transformed from marine deposits to continental deposits.Figure 1
(a) Paleogeographic sketch map of the mid-Eocene in the Tethyan realm (modified from [31, 32]); (b) Eocene paleogeographic map of the Tarim Plate (modified from [33]).
(a)(b)The Kuqa Basin is a secondary basin adjacent to the southern Tianshan Mountains in the northern part of the Tarim Basin, and it extends in a nearly east-west direction [34, 35] (Figure 2). The stable tectonic environment created favorable depositional conditions for the formation of the Paleogene evaporite series. The deposition center was located in the central and western parts of the basin, and huge thick salt-bearing strata formed. Paleocene and Eocene strata are composed of the Talak and Xiaokuzibai Formations of the Kumugeliemu Group. Marine fossils (such as foraminifera and gastropods) have been found at the bottom of the Talak Formation; the Xiaokuzibai Formation is composed of purple-red sandstone, silty mudstone, limestone, brown-red silty mudstone, and thick gypsum rock and rock salt deposits, and marine microfossils are found in the middle part [36]. Zheng and Meng [37] established the precise magnetostratigraphy of Paleogene strata in the Kuqa Basin based on paleomagnetic data and determined the ages of the top and bottom of the Kumgeliemu Group, which are 38 Ma and 60.5 Ma, respectively. Teng et al. [38] and Li et al. [39] also proposed that the age of the boundary between the Paleogene Kumgeliemu Group and the Oligocene Suwei Formation is 38 Ma. Cao et al. [40] identified and compared Paleogene evaporite sedimentary cycles in the Kuqa Basin based on multiple drilling data from the Tarim Oilfield Company and developed a standard stratigraphic section of evaporite sedimentary cycles. Therefore, the formation age of salt-bearing strata from borehole DZK01 can be preliminarily determined to be middle Eocene.Figure 2
Simplified geological map of the Kuqa Basin [41].


## 3. Materials and Experimental Procedure

### 3.1. Materials

Rock salt samples used to measureTh and the chemical compositions of fluid inclusions were collected from middle Eocene salt-bearing strata in borehole DZK01 (Figure 1). Borehole DZK01 is located in the northeastern Baicheng depression of the Kuqa Basin, and this is the first scientific research borehole in the basin to find potash deposits. The borehole mainly comprises mud-bearing rock salt, rock salt with gypsum and mud, gypsum-bearing argillaceous rock salt, and mud-bearing gypsiferous rock salt (Figures 3(a) and 3(b)).Figure 3
Characteristics of evaporite lithology and halite fluid inclusions from borehole DZK01 in the Kuqa Basin. (a) Gypsum rock with maroon boulder clay; (b) pure rock salt and rock salt with maroon boulder clay; (c, d) primary band-like fluid inclusions developed along growth faces of halite crystals and pits left on the surface of halite after laser ablation.
(a)(b)(c)(d)Borehole samples were carefully selected, and the size, shape, and distribution characteristics of fluid inclusions were observed under a microscope and recorded to distinguish between primary and secondary fluid inclusions. Since halite with primary fluid inclusions is the most direct evidence to verify its originality, we placed selected primary halite samples into a desiccant for storage. Primary halite crystals are characterized by euhedral textures, and white smoky or cloudy, fluid inclusions are distributed along the growth surfaces of halite crystals in directional and regular strips. The sizes of individual inclusions vary, with diameters in the range of ~3 to 60μm, and the inclusions are dominated by single-phase liquid inclusions, with few or no two-phase gas-liquid or three-phase gas-liquid-solid inclusions containing daughter crystals.


### 3.2. Experimental Procedure

TheTh values of halite fluid inclusions were measured at the State Key Laboratory of Nuclear Resources and Environment, East China University of Technology. A Linkam THMS600 instrument (made in England) was used, and the measured temperature range was at −196 to +600°C. The accuracies of freezing and Th data were ±0.1°C and ±0.5°C, respectively. Before using cooling nucleation to measure Th, we used a small hammer to split halite crystals along their cleavage planes into approximately 1 mm-thick slices. First, the halite cleavage slices were carefully observed under a microscope and photographs were taken to record all single-phase liquid fluid inclusions. Then, the selected cleavage slices were placed into a refrigerator (at −15°C to −20°C) for one week and the slices were quickly moved from the refrigerator to a prepared heating and cooling stage and frozen at −18°C until artificial nucleation bubbles appeared within the fluid inclusions. The initial heating rate was set to 0.5°C/min and then slowed to 0.1°C/min nearing 10°C until all observed artificial nucleation bubbles disappeared. Roberts and Spence [13] noted that the Th of bubbles existing before cooling was abnormally high. Therefore, we chose fluid inclusions that featured artificial nucleation after cooling as the research subjects.The determination of the chemical compositions of halite fluid inclusions was completed at the National Research Center for Geoanalysis. The laser ablation inductively coupled plasma mass spectrometry (LA-ICP-MS) method was used, and an Element 2 ICP mass spectrometer (Finnigan, Germany) and UP 213 laser (New Wave Company) were used. The diameter of the laser beam was 25μm, the laser wavelength was 213 nm, and the pulse duration was 4 ns. Under laser ablation sampling conditions, high-purity helium gas was used as the carrier gas to optimize ablation and transmission efficiency. The actual energy acting on the samples was controlled between 0.03 and 0.06 mJ during the experiment, and the ablation energy density was controlled between 7 and 14 J/cm2. Using the point ablation mode, the gas background acquisition time of each analysis point was approximately 15 s, and the signal acquisition time was 45 s. The calibration method involved internal standard-external standard combination methods [42, 43].


#### 3.2.1. External Standard Method

The prepared standard solution was drawn into a pure quartz capillary tube and quickly sealed with epoxy resin. During the test and analysis, manufactured artificial fluid inclusions were attached to a glass sheet with double-sided adhesive and put into the laser ablation sample chamber together with test samples.


#### 3.2.2. Internal Standard Method

Na was selected as the internal standard element for halite fluid inclusion samples, and the Na content was calculated to be at 141.62 g/L based on the theoretical value. The relative sensitivity between the standard calibration instrument and elements in the unknown sample was assumed to remain unchanged, that is, calibration was carried out according to the consistency of changes in the internal standard element and the elements to be measured [42, 44].Figures3(c) and 3(d) show fluid inclusions after laser ablation. Figure 4 shows the variation curve of the mass spectrum signal intensity with time during the analysis of typical halite fluid inclusions. From 1 to 14 s, the measured signal intensity is the background value; the signal intensities of the major elements Na, K, Mg, and Ca are very stable, and the signal intensities of trace elements Rb, Sr, and B fluctuate slightly. At 15 s, the signal intensities of Na, Mg, and Sr increase instantly and those of other elements remain stable; this is the result of laser ablation reaching the halite surface and releasing Na, Mg, and Sr. Then, the signal intensity of Na decreases slightly and the signal intensities of the other elements decrease quickly to the initial background values. From 26 to 33 s, when laser ablation reaches the fluid inclusion, the signal intensities of all major and trace elements increase significantly, especially K, Mg, Ca, and Sr. The signal intensities of these elements remain high for 7 s, indicating that there is abundant fluid available for ablation and that the inclusion is large.Figure 4
Mass spectral signal intensity versus time for a single fluid inclusion in halite (no. 4 fluid inclusion from 1385 m).


## 3.1. Materials

Rock salt samples used to measureTh and the chemical compositions of fluid inclusions were collected from middle Eocene salt-bearing strata in borehole DZK01 (Figure 1). Borehole DZK01 is located in the northeastern Baicheng depression of the Kuqa Basin, and this is the first scientific research borehole in the basin to find potash deposits. The borehole mainly comprises mud-bearing rock salt, rock salt with gypsum and mud, gypsum-bearing argillaceous rock salt, and mud-bearing gypsiferous rock salt (Figures 3(a) and 3(b)).Figure 3
Characteristics of evaporite lithology and halite fluid inclusions from borehole DZK01 in the Kuqa Basin. (a) Gypsum rock with maroon boulder clay; (b) pure rock salt and rock salt with maroon boulder clay; (c, d) primary band-like fluid inclusions developed along growth faces of halite crystals and pits left on the surface of halite after laser ablation.
(a)(b)(c)(d)Borehole samples were carefully selected, and the size, shape, and distribution characteristics of fluid inclusions were observed under a microscope and recorded to distinguish between primary and secondary fluid inclusions. Since halite with primary fluid inclusions is the most direct evidence to verify its originality, we placed selected primary halite samples into a desiccant for storage. Primary halite crystals are characterized by euhedral textures, and white smoky or cloudy, fluid inclusions are distributed along the growth surfaces of halite crystals in directional and regular strips. The sizes of individual inclusions vary, with diameters in the range of ~3 to 60μm, and the inclusions are dominated by single-phase liquid inclusions, with few or no two-phase gas-liquid or three-phase gas-liquid-solid inclusions containing daughter crystals.


## 3.2. Experimental Procedure

TheTh values of halite fluid inclusions were measured at the State Key Laboratory of Nuclear Resources and Environment, East China University of Technology. A Linkam THMS600 instrument (made in England) was used, and the measured temperature range was at −196 to +600°C. The accuracies of freezing and Th data were ±0.1°C and ±0.5°C, respectively. Before using cooling nucleation to measure Th, we used a small hammer to split halite crystals along their cleavage planes into approximately 1 mm-thick slices. First, the halite cleavage slices were carefully observed under a microscope and photographs were taken to record all single-phase liquid fluid inclusions. Then, the selected cleavage slices were placed into a refrigerator (at −15°C to −20°C) for one week and the slices were quickly moved from the refrigerator to a prepared heating and cooling stage and frozen at −18°C until artificial nucleation bubbles appeared within the fluid inclusions. The initial heating rate was set to 0.5°C/min and then slowed to 0.1°C/min nearing 10°C until all observed artificial nucleation bubbles disappeared. Roberts and Spence [13] noted that the Th of bubbles existing before cooling was abnormally high. Therefore, we chose fluid inclusions that featured artificial nucleation after cooling as the research subjects.The determination of the chemical compositions of halite fluid inclusions was completed at the National Research Center for Geoanalysis. The laser ablation inductively coupled plasma mass spectrometry (LA-ICP-MS) method was used, and an Element 2 ICP mass spectrometer (Finnigan, Germany) and UP 213 laser (New Wave Company) were used. The diameter of the laser beam was 25μm, the laser wavelength was 213 nm, and the pulse duration was 4 ns. Under laser ablation sampling conditions, high-purity helium gas was used as the carrier gas to optimize ablation and transmission efficiency. The actual energy acting on the samples was controlled between 0.03 and 0.06 mJ during the experiment, and the ablation energy density was controlled between 7 and 14 J/cm2. Using the point ablation mode, the gas background acquisition time of each analysis point was approximately 15 s, and the signal acquisition time was 45 s. The calibration method involved internal standard-external standard combination methods [42, 43].


### 3.2.1. External Standard Method

The prepared standard solution was drawn into a pure quartz capillary tube and quickly sealed with epoxy resin. During the test and analysis, manufactured artificial fluid inclusions were attached to a glass sheet with double-sided adhesive and put into the laser ablation sample chamber together with test samples.


### 3.2.2. Internal Standard Method

Na was selected as the internal standard element for halite fluid inclusion samples, and the Na content was calculated to be at 141.62 g/L based on the theoretical value. The relative sensitivity between the standard calibration instrument and elements in the unknown sample was assumed to remain unchanged, that is, calibration was carried out according to the consistency of changes in the internal standard element and the elements to be measured [42, 44].Figures3(c) and 3(d) show fluid inclusions after laser ablation. Figure 4 shows the variation curve of the mass spectrum signal intensity with time during the analysis of typical halite fluid inclusions. From 1 to 14 s, the measured signal intensity is the background value; the signal intensities of the major elements Na, K, Mg, and Ca are very stable, and the signal intensities of trace elements Rb, Sr, and B fluctuate slightly. At 15 s, the signal intensities of Na, Mg, and Sr increase instantly and those of other elements remain stable; this is the result of laser ablation reaching the halite surface and releasing Na, Mg, and Sr. Then, the signal intensity of Na decreases slightly and the signal intensities of the other elements decrease quickly to the initial background values. From 26 to 33 s, when laser ablation reaches the fluid inclusion, the signal intensities of all major and trace elements increase significantly, especially K, Mg, Ca, and Sr. The signal intensities of these elements remain high for 7 s, indicating that there is abundant fluid available for ablation and that the inclusion is large.Figure 4
Mass spectral signal intensity versus time for a single fluid inclusion in halite (no. 4 fluid inclusion from 1385 m).


## 3.2.1. External Standard Method

The prepared standard solution was drawn into a pure quartz capillary tube and quickly sealed with epoxy resin. During the test and analysis, manufactured artificial fluid inclusions were attached to a glass sheet with double-sided adhesive and put into the laser ablation sample chamber together with test samples.


## 3.2.2. Internal Standard Method

Na was selected as the internal standard element for halite fluid inclusion samples, and the Na content was calculated to be at 141.62 g/L based on the theoretical value. The relative sensitivity between the standard calibration instrument and elements in the unknown sample was assumed to remain unchanged, that is, calibration was carried out according to the consistency of changes in the internal standard element and the elements to be measured [42, 44].Figures3(c) and 3(d) show fluid inclusions after laser ablation. Figure 4 shows the variation curve of the mass spectrum signal intensity with time during the analysis of typical halite fluid inclusions. From 1 to 14 s, the measured signal intensity is the background value; the signal intensities of the major elements Na, K, Mg, and Ca are very stable, and the signal intensities of trace elements Rb, Sr, and B fluctuate slightly. At 15 s, the signal intensities of Na, Mg, and Sr increase instantly and those of other elements remain stable; this is the result of laser ablation reaching the halite surface and releasing Na, Mg, and Sr. Then, the signal intensity of Na decreases slightly and the signal intensities of the other elements decrease quickly to the initial background values. From 26 to 33 s, when laser ablation reaches the fluid inclusion, the signal intensities of all major and trace elements increase significantly, especially K, Mg, Ca, and Sr. The signal intensities of these elements remain high for 7 s, indicating that there is abundant fluid available for ablation and that the inclusion is large.Figure 4
Mass spectral signal intensity versus time for a single fluid inclusion in halite (no. 4 fluid inclusion from 1385 m).


## 4. Results

Approximately 15% of single-phase liquid fluid inclusions generated artificial nucleation vapor bubbles after cooling. In total, 220Th values were measured from artificially nucleated vapor bubbles in primary halite crystals from borehole DZK01 (Table 1) and the Th values of the four stratigraphic intervals range from 11.1 to 47.1°C (S4, 1363 m), 13.2 to 52.3°C (S3, 1373 m), 15.3 to 36.2°C (S2,1382 m), and 9.4 to 54.1°C (S1, 1470 m). The corresponding average Th values are 27.2°C, 31.2°C, 23.2°C, and 30.5°C. In this paper, each inclusion-rich band is regarded as an individual fluid inclusion assemblage (FIA) [46], showing that all primary fluid inclusions near the FIA formed almost simultaneously. The Th range within each FIA is within 15°C, and 84% of FIAs have a range of less than 10°C. The Th range measured within all FIAs yields an average value of 8.0°C, with a maximum value of 11.7°C and a minimum value of 4.6°C.Table 1
Th (°C) of middle Eocene halite primary fluid inclusions in borehole DZK01, Kuqa Basin.
SampleDepth (m)Th (°C)/size (μm)ThMAX (°C)ThMIN (°C)ThAVG (°C)ThRANGE (°C)S1136347.111.127.2FIA 111.1/16; 13.8/15; 14.1/29; 16.4/28; 17.2/28; 17.8/24; 18.1/20; 18.8/227.7FIA 219.5/22; 20.1/26; 20.5/18; 20.8/8; 21.3/12; 21.5/13; 22.2/15; 22.4/36; 22.6/42; 23.8/8; 24.1/6; 24.1/29; 24.2/28; 24.9/15; 25.1/195.6FIA 322.8/19; 23.7/10; 24.4/32; 24.6/16; 24.7/25; 28.3/22; 28.4/19; 28.5/28; 28.6/31; 28.7/305.9FIA 425.6/18; 26.3/33; 26.5/34; 26.7/20; 29.2/31; 30.2/21; 30.2/28; 30.3/20; 31.3/185.7FIA 530.8/16; 31.2/16; 31.5/17; 31.5/15; 31.6/19; 31.7/25; 31.7/15; 32.3/10; 33.2/18; 33.6/14; 33.8/10; 35.4/264.6FIA 637.2/10; 37.3/11; 39.9/16; 41.6/15; 42.7/23; 44.8/29; 47.1/189.9S2137352.313.231.2FIA 113.2/27; 14.5/26; 14.6/23; 15.1/20; 15.5/19; 19.5/14; 21.2/34; 22.1/388.9FIA 220.8/18; 21.0/10; 23.4/41; 28.9/28; 29.5/27; 29.6/24; 29.6/238.8FIA 329.1/16; 29.8/25; 34.1/28; 34.2/12; 34.5/13; 35.1/18; 35.2/166.1FIA 435.3/26; 38.1/28; 38.1/23; 38.4/16; 45.6/2010.3FIA 542.6/14; 45.8/7; 46.4/22; 47.6/19; 49.2/15; 52.3/319.7S3138236.215.323.2FIA 115.3/24; 16.3/10; 16.4/9; 16.4/35; 16.6/33; 16.7/24; 17.2/26; 17.5/23; 17.6/18; 17.8/14; 18.4/10; 18.8/27; 19.1/28; 19.3/28; 19.5/25; 19.6/17; 19.6/16; 19.8/27; 20.5/8; 20.8/11; 22.3/19; 22.8/24; 23.8/258.5FIA 224.3/12; 24.3/18; 24.5/31; 24.8/48; 25.1/26; 26.1/27; 26.2/16; 27.3/29; 27.6/33; 31.4/157.1FIA 328.9/15; 31.2/14; 31.6/31; 31.6/32; 31.6/18; 32.7/26; 32.8/28; 36.2/207.3S4147054.19.430.5FIA 19.4/24; 10.2/23; 14.5/25; 15.6/28; 15.7/12; 16.2/20; 16.3/28; 16.7/24; 17.3/33; 17.5/38; 17.8/36; 19.5/31; 20.7/46; 20.8/41; 21.1/2711.7FIA 222.1/35; 22.2/24; 22.8/28; 23.1/24; 24.1/26; 24.3/15; 25.1/24; 25.9/16; 26.1/26; 26.2/17; 26.3/25; 26.5/26; 26.7/33; 27.2/37; 27.2/35; 27.8/26; 27.8/8; 28.1/8; 28.2/7; 28.5/24; 29.3/18; 29.3/23; 29.4/25; 30.1/298.0FIA 328.6/25; 28.9/15; 29.1/19; 30.2/38; 30.2/44; 30.3/35; 30.4/21; 30.5/20; 31.1/17; 31.7/22; 31.9/28; 32.4/23; 32.4/14; 32.5/15; 32.7/22; 32.8/10; 33.2/33; 34.5/29; 34.6/14; 35.4/41; 36.1/18; 36.4/22; 36.5/31; 36.6/27; 36.8/20; 37.6/31; 37.8/15; 38.1/245.7FIA 435.5/37; 35.6/34; 35.8/36; 38.4/16; 38.5/28; 40.8/24; 41.6/35; 41.8/10; 42.1/18; 44.8/27; 46.1/16; 46.1/2810.6FIA 544.5/20; 45.3/26; 46.4/24; 47.6/23; 52.4/20; 54.1/299.6ThMAX: maximum homogenization temperature; ThMIN: minimum homogenization temperature; ThAVG: average homogenization temperature; ThRANGE: range of Th data; FIA: fluid inclusion assemblage.The chemical compositions of 22 fluid inclusions from 10 rock salt samples were determined by LA-ICP-MS (Table2), and their sizes ranged from ~30×20μm to 80×30μm. The chemical compositions of fluid inclusions in the same sample are quite different. Based on petrographic observations under the microscope, they come from different halite crystals in the same sample and information on paleobrine from different stages is captured during halite crystallization, such as the no. 18 and no. 19 fluid inclusions.Table 2
Ion concentrations in halite fluid inclusions from borehole DZK01 in the Kuqa Basin.
Depth (m)Inclusion no.ρ (B)/(g/L)ρ (B)/(mg/L)K+Ca2+Mg2+Li+B+Rb+Sr2+Br-137010.231.160.420.121.620.4423.5212.64137320.114.210.190.862.600.00138.0812.56137430.120.170.1300.980.074.742.55138540.470.060.090.050.750.310.805.08141550.263.090.531.801.180.15115.8910.33143561.250.060.060.551.763.350.6615.2570.300.040.031.230.521.940.546.4180.280.020.020.440.160.380.113.11143690.270.020.010.060.070.260.166.06100.120.220.080.520.180.067.563.35110.070.050.050.270.190.130.944.721469120.340.350.160.400.270.097.562.83130.100.650.100.040.120.0517.393.651476140.120.230.010.010.440.080.1018.00150.270.680.130.150.040.0515.627.45160.220.020.010.220.270.180.252.53170.140.780.200.440.160.0416.174.07180.412.540.570.520.400.2072.3411.49193.070.460.866.6734.0910.623.3248.52202.910.310.522.2111.534.101.4053.131478210.710.110.150.372.650.400.847.05220.130.850.050.120.080.1324.024.21


## 5. Discussion

### 5.1. Reliability and Stability ofTh Data

Damage or recrystallization occurs easily during burial and at depth due to the deliquescent and solubility nature of rock salt and can affect the reliability and stability ofTh data, especially for ancient rock salt samples. The Th data do not require pressure correction because rock salt forms in a shallow depositional environment and the temperatures captured by fluid inclusions under low-pressure conditions are approximately equal to Th, thus providing a direct record of temperature during rock salt deposition. Primary fluid inclusions from the same inclusion growth band were captured contemporaneously [45]. However, multiple inclusion bands in primary halite crystals were not formed contemporaneously. Therefore, Th data obtained from different inclusion bands are also diverse [45].We use two methods to verify whether primary fluid inclusions have undergone damage or alteration from thermal reequilibration: thermal reequilibration analysis of theTh data and evaluation of the relationship between the size and Th of fluid inclusions. On the one hand, the consistency of the Th data from individual FIAs can be used as an indicator for evaluating thermal reequilibration [45]. Goldstein and Reynolds [46] noted that approximately 90% of Th data in individual FIAs have a fluctuation range of less than 15°C, indicating that primary fluid inclusions have not undergone alteration from thermal reequilibration. The Th data in this paper meet this criterion (Table 1), as the temperature ranges of all Th data from 19 FIAs are less than 15°C, with a minimum of 4.6°C and a maximum of 11.7°C. Therefore, the halite crystals have not been affected by thermal reequilibration. Furthermore, the relationship between the size and Th of fluid inclusions can be used as another indicator to determine whether fluid inclusions have been affected by thermal reequilibration. Large inclusions are more extendable than small inclusions, and fluid inclusions undergoing extension have a higher Th than the original temperature at the time of formation [47]. In other words, if inclusions have undergone extension, large inclusions are more likely to produce higher Th values than small inclusions. Our results show that there is no correlation between the size of fluid inclusions and the corresponding Th (Figure 5). Therefore, thermal reequilibration did not alter or damage halite crystals, which further supports the rationality and stability of the Th data. The Th data from middle Eocene rock salt from borehole DZK01 may accurately reflect the brine temperatures during salt formation.Figure 5
Crossplot of theTh data against the size of fluid inclusions.


### 5.2. Significance of Paleobrine Temperature

The temperature of the brine during the salt-forming period can be directly and quantitatively reconstructed from theTh values of halite fluid inclusions [15, 16, 48]. In addition, previous studies on modern salt lakes and laboratory halite crystals have shown that the highest Th values of halite fluid inclusions are approximately equal to the highest brine temperature during the halite crystallization process [14, 45, 49]. Our results show that the Th values of the 4 salt-bearing intervals are generally high (Figure 6), with an average value of 28.3°C and a maximum temperature of 54.1°C, which represent the average and high-temperature brine characteristics in the Kuqa Basin in the middle Eocene. Bougeois et al. [50] conducted a study on marine oyster fossils in the southwestern part of the Tarim Basin and showed that the average sea surface temperature during the middle Eocene was approximately 27–28°C. Therefore, the evidence supports our inference based on Th data and indicates that our Th data in the middle Eocene Kuqa Basin are reliable and reasonable.Figure 6
Th data characteristics of primary fluid inclusions from middle Eocene halite in borehole DZK01, Kuqa Basin.Zhao et al. [17] studied halite fluid inclusions from 8 salt-bearing basins in China and other countries and used the Th values to estimate the evaporation rate of ancient salt lakes, and the results showed that extremely high-temperature conditions (water and air temperatures) are conducive to rapidly concentrating salt lake brine, shortening the time interval from salt formation to potash formation, which is beneficial to the formation of potash deposits. Liu et al. [51] proposed that a hot and dry climate is a prerequisite for potash formation by ancient salt lake evaporation. The formation of many ancient and modern potash deposits is closely related to high-temperature paleobrine environments. For example, the highest paleobrine temperature of potash deposits in the Silurian Michigan Basin is 59°C [52], the highest paleobrine temperature of potash deposits in the Middle Cretaceous Korat Plateau is 62.1°C [53], and the highest paleobrine temperature of Quaternary Lop Nur potash deposits in the Tarim Basin is 58°C [54]. Therefore, the high-temperature conditions experienced during the middle Eocene salt-forming period in the Kuqa Basin may indicate relatively rapid evaporation rates. Moreover, potassium minerals, such as sylvite, carnallite, and syngenite, have been discovered in this stratum [55], indicating that the salt lake brine experienced high degrees of evaporation and concentration under the high-temperature conditions required for potash formation.


### 5.3. Significance of the Chemical Composition of Paleobrine

The elements K and Rb and the elements Sr and Ca have similar chemical properties, and they often displace each other in an isomorphic manner during continuous evaporation and the concentration of salt-forming brine. In addition, K is positively correlated with Mg and Br [56, 57]. Therefore, the linear relationships between K+ and Mg2+, K+ and Rb+, K+ and Br-, and Ca2+ and Sr2+ are often used to indicate the reliability of measured data [23, 58]. The ion concentrations that we tested showed good positive correlations (Figure 7), conforming to the evaporation and concentration patterns of salt lake brine, indicating that our data have good reliability and validity.Figure 7
The relationships between K+ and Mg2+, Rb+ and Br-, and Sr2+ and Ca2+ in halite fluid inclusions from 1476 m in borehole DZK01.The chemical compositions of halite fluid inclusions are characterized by high Ca2+ and Sr2+ concentrations, which may be due to the supply of terrestrial fresh water involved in the salinization process. Zhang et al. [12] and Xu et al. [59] systematically analyzed the carbon, oxygen, sulfur, and strontium isotope compositions of middle Eocene carbonate rocks and sulfate rocks and found that the provenance in the salt-forming environment was mostly a mixture of marine and continental sediments. The Br− data from that study are compared with the chemical analysis results for the rock salt from borehole DZK01 [60], and the Br− content in the latter is lower than the detection limit, whereas the Br− content in the former is higher than the detection limit. This pattern is determined by the chemical properties of Br because Br rarely enters the crystal lattice of salt minerals but is present mainly in the form of brine.The concentrations of other ions in the no. 19 and no. 20 fluid inclusions from the 1476 m halite sample are all the maximum values except for Ca2+ and Sr2+; there are two reasons for this. On the one hand, salt lake brine generally undergoes evaporative concentration and desalination caused by the mixing of external water bodies during the evolution process. At 1476 m, the brine evaporates and evolves to a higher concentration stage and the concentrations of K+, Mg2+, Rb+, and Br− increase accordingly. In addition, a previous work discovered potassium minerals at 1476 m at the bottom of the borehole, which also confirmed the high degrees of evaporation and concentration of brine. On the other hand, due to the large sample collection interval, these ion concentrations did not show a good transitional relationship, indicating that the ion concentrations of inclusion nos. 19 and 20 differ greatly from those of other inclusions. The K+ concentrations in the no. 19 and no. 20 fluid inclusions reach 3.07 g/L and 2.91 g/L, respectively, corresponding to KCl contents of 0.59% and 0.56%, respectively. Li et al. [61], based on the “specifications for salt lakes, salt mineral exploration (DZ/T0212—2002),”, systematically collected recent survey results and research data on potassium-rich brine and summarized and determined the lowest industrial grade of potassium-rich brine (KCl≥0.5%). It can be inferred that the evolution phase of ancient brine in the basin reached the stage of potash formation. In addition, Wu et al. [60] conducted a chemical analysis of rock salt samples from different depths in borehole DZK01 and showed that the rock salt at the bottom of the borehole has a high content of K+, with a maximum of 0.34%. Xu et al. [55] studied the hydrogen and oxygen isotopes of primary fluid inclusions in halite from borehole DZK01 and found that the salt-bearing strata at the bottom of the borehole had experienced a high degree of evaporation and that large amounts of potassium minerals precipitated. The interval that has good potential for potassium mineral formation is inferred to have good potential for potash formation. This is consistent with the K+ concentration characteristics of halite fluid inclusions studied in this paper and further shows that brine had high degrees of evaporation and concentration in the early salt-forming period and reached the potassium-forming stage.


## 5.1. Reliability and Stability ofTh Data

Damage or recrystallization occurs easily during burial and at depth due to the deliquescent and solubility nature of rock salt and can affect the reliability and stability ofTh data, especially for ancient rock salt samples. The Th data do not require pressure correction because rock salt forms in a shallow depositional environment and the temperatures captured by fluid inclusions under low-pressure conditions are approximately equal to Th, thus providing a direct record of temperature during rock salt deposition. Primary fluid inclusions from the same inclusion growth band were captured contemporaneously [45]. However, multiple inclusion bands in primary halite crystals were not formed contemporaneously. Therefore, Th data obtained from different inclusion bands are also diverse [45].We use two methods to verify whether primary fluid inclusions have undergone damage or alteration from thermal reequilibration: thermal reequilibration analysis of theTh data and evaluation of the relationship between the size and Th of fluid inclusions. On the one hand, the consistency of the Th data from individual FIAs can be used as an indicator for evaluating thermal reequilibration [45]. Goldstein and Reynolds [46] noted that approximately 90% of Th data in individual FIAs have a fluctuation range of less than 15°C, indicating that primary fluid inclusions have not undergone alteration from thermal reequilibration. The Th data in this paper meet this criterion (Table 1), as the temperature ranges of all Th data from 19 FIAs are less than 15°C, with a minimum of 4.6°C and a maximum of 11.7°C. Therefore, the halite crystals have not been affected by thermal reequilibration. Furthermore, the relationship between the size and Th of fluid inclusions can be used as another indicator to determine whether fluid inclusions have been affected by thermal reequilibration. Large inclusions are more extendable than small inclusions, and fluid inclusions undergoing extension have a higher Th than the original temperature at the time of formation [47]. In other words, if inclusions have undergone extension, large inclusions are more likely to produce higher Th values than small inclusions. Our results show that there is no correlation between the size of fluid inclusions and the corresponding Th (Figure 5). Therefore, thermal reequilibration did not alter or damage halite crystals, which further supports the rationality and stability of the Th data. The Th data from middle Eocene rock salt from borehole DZK01 may accurately reflect the brine temperatures during salt formation.Figure 5
Crossplot of theTh data against the size of fluid inclusions.


## 5.2. Significance of Paleobrine Temperature

The temperature of the brine during the salt-forming period can be directly and quantitatively reconstructed from theTh values of halite fluid inclusions [15, 16, 48]. In addition, previous studies on modern salt lakes and laboratory halite crystals have shown that the highest Th values of halite fluid inclusions are approximately equal to the highest brine temperature during the halite crystallization process [14, 45, 49]. Our results show that the Th values of the 4 salt-bearing intervals are generally high (Figure 6), with an average value of 28.3°C and a maximum temperature of 54.1°C, which represent the average and high-temperature brine characteristics in the Kuqa Basin in the middle Eocene. Bougeois et al. [50] conducted a study on marine oyster fossils in the southwestern part of the Tarim Basin and showed that the average sea surface temperature during the middle Eocene was approximately 27–28°C. Therefore, the evidence supports our inference based on Th data and indicates that our Th data in the middle Eocene Kuqa Basin are reliable and reasonable.Figure 6
Th data characteristics of primary fluid inclusions from middle Eocene halite in borehole DZK01, Kuqa Basin.Zhao et al. [17] studied halite fluid inclusions from 8 salt-bearing basins in China and other countries and used the Th values to estimate the evaporation rate of ancient salt lakes, and the results showed that extremely high-temperature conditions (water and air temperatures) are conducive to rapidly concentrating salt lake brine, shortening the time interval from salt formation to potash formation, which is beneficial to the formation of potash deposits. Liu et al. [51] proposed that a hot and dry climate is a prerequisite for potash formation by ancient salt lake evaporation. The formation of many ancient and modern potash deposits is closely related to high-temperature paleobrine environments. For example, the highest paleobrine temperature of potash deposits in the Silurian Michigan Basin is 59°C [52], the highest paleobrine temperature of potash deposits in the Middle Cretaceous Korat Plateau is 62.1°C [53], and the highest paleobrine temperature of Quaternary Lop Nur potash deposits in the Tarim Basin is 58°C [54]. Therefore, the high-temperature conditions experienced during the middle Eocene salt-forming period in the Kuqa Basin may indicate relatively rapid evaporation rates. Moreover, potassium minerals, such as sylvite, carnallite, and syngenite, have been discovered in this stratum [55], indicating that the salt lake brine experienced high degrees of evaporation and concentration under the high-temperature conditions required for potash formation.


## 5.3. Significance of the Chemical Composition of Paleobrine

The elements K and Rb and the elements Sr and Ca have similar chemical properties, and they often displace each other in an isomorphic manner during continuous evaporation and the concentration of salt-forming brine. In addition, K is positively correlated with Mg and Br [56, 57]. Therefore, the linear relationships between K+ and Mg2+, K+ and Rb+, K+ and Br-, and Ca2+ and Sr2+ are often used to indicate the reliability of measured data [23, 58]. The ion concentrations that we tested showed good positive correlations (Figure 7), conforming to the evaporation and concentration patterns of salt lake brine, indicating that our data have good reliability and validity.Figure 7
The relationships between K+ and Mg2+, Rb+ and Br-, and Sr2+ and Ca2+ in halite fluid inclusions from 1476 m in borehole DZK01.The chemical compositions of halite fluid inclusions are characterized by high Ca2+ and Sr2+ concentrations, which may be due to the supply of terrestrial fresh water involved in the salinization process. Zhang et al. [12] and Xu et al. [59] systematically analyzed the carbon, oxygen, sulfur, and strontium isotope compositions of middle Eocene carbonate rocks and sulfate rocks and found that the provenance in the salt-forming environment was mostly a mixture of marine and continental sediments. The Br− data from that study are compared with the chemical analysis results for the rock salt from borehole DZK01 [60], and the Br− content in the latter is lower than the detection limit, whereas the Br− content in the former is higher than the detection limit. This pattern is determined by the chemical properties of Br because Br rarely enters the crystal lattice of salt minerals but is present mainly in the form of brine.The concentrations of other ions in the no. 19 and no. 20 fluid inclusions from the 1476 m halite sample are all the maximum values except for Ca2+ and Sr2+; there are two reasons for this. On the one hand, salt lake brine generally undergoes evaporative concentration and desalination caused by the mixing of external water bodies during the evolution process. At 1476 m, the brine evaporates and evolves to a higher concentration stage and the concentrations of K+, Mg2+, Rb+, and Br− increase accordingly. In addition, a previous work discovered potassium minerals at 1476 m at the bottom of the borehole, which also confirmed the high degrees of evaporation and concentration of brine. On the other hand, due to the large sample collection interval, these ion concentrations did not show a good transitional relationship, indicating that the ion concentrations of inclusion nos. 19 and 20 differ greatly from those of other inclusions. The K+ concentrations in the no. 19 and no. 20 fluid inclusions reach 3.07 g/L and 2.91 g/L, respectively, corresponding to KCl contents of 0.59% and 0.56%, respectively. Li et al. [61], based on the “specifications for salt lakes, salt mineral exploration (DZ/T0212—2002),”, systematically collected recent survey results and research data on potassium-rich brine and summarized and determined the lowest industrial grade of potassium-rich brine (KCl≥0.5%). It can be inferred that the evolution phase of ancient brine in the basin reached the stage of potash formation. In addition, Wu et al. [60] conducted a chemical analysis of rock salt samples from different depths in borehole DZK01 and showed that the rock salt at the bottom of the borehole has a high content of K+, with a maximum of 0.34%. Xu et al. [55] studied the hydrogen and oxygen isotopes of primary fluid inclusions in halite from borehole DZK01 and found that the salt-bearing strata at the bottom of the borehole had experienced a high degree of evaporation and that large amounts of potassium minerals precipitated. The interval that has good potential for potassium mineral formation is inferred to have good potential for potash formation. This is consistent with the K+ concentration characteristics of halite fluid inclusions studied in this paper and further shows that brine had high degrees of evaporation and concentration in the early salt-forming period and reached the potassium-forming stage.


## 6. Conclusions

(1)
TheTh data of measured primary halite fluid inclusions are accurate and reasonable, and these data can quantitatively reconstruct the temperature of salt-forming brine in the Kuqa Basin in the middle Eocene. The Th of 220 fluid inclusions ranges from 9.4 to 54.1°C, reflecting a high-temperature brine environment that was conducive to the rapid deposition of potassium minerals(2)
The KCl content of salt-forming brine at the bottom of the borehole can reach up to 0.59%, which is higher than the lowest industrial grade of potassium-rich brine KCl (0.5%). Combined with previous research work, these results further show that salt-forming brine had high degrees of evaporation and concentration and reached the potash-forming stage



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*Source: 5574772-2021-03-10.xml*