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Article(id=1307086910220956060, tenantId=1146029695717560320, journalId=1306274195778404443, issueId=1307086317918122434, articleNumber=null, orderNo=null, doi=10.12401/j.nwg.2025171, pmid=null, cstr=null, oa=null, hot=null, price=null, onlineType=0, articleFormat=0, articleType=null, articleTypeStr=null, receivedDate=1768838400000, receivedDateStr=2026-01-20, revisedDate=1770220800000, revisedDateStr=2026-02-05, acceptedDate=1770480000000, acceptedDateStr=2026-02-08, onlineDate=1789563403896, onlineDateStr=2026-09-16, pubDate=1776614400000, pubDateStr=2026-04-20, doiRegisterDate=null, doiRegisterDateStr=null, onlineIssueDate=1789563403896, onlineIssueDateStr=2026-09-16, onlineJustAcceptDate=null, onlineJustAcceptDateStr=null, onlineFirstDate=null, onlineFirstDateStr=null, sourceXml=null, magXml=null, createTime=1789563403896, creator=13701087609, updateTime=1789563403896, updator=13701087609, issue=Issue{id=1307086317918122434, tenantId=1146029695717560320, journalId=1306274195778404443, year='2026', volume='59', issue='2', pageStart='1', pageEnd='328', issueExtLink='null', onlineDate='null', pubDate='1776614400000', pubDateStr='2026-04-20', beforeIssueId=null, nextIssueId=null, price=null, status=1, issueComplete=1, articleOrder=1, issueType=-1, specialIssue=null, createTime=1789563262680, creator='13701087609', updateTime=1789616239746, updator='13701087609', preIssue=null, nextIssue=null, articleTotal=null, ext={EN=IssueExt(id=1307308519917638393, tenantId=1146029695717560320, journalId=1306274195778404443, issueId=1307086317918122434, language=EN, specialIssueTitle=, coverIllustrator=null, specialIssueEditor=, specialIssueAbout=), CN=IssueExt(id=1307308519917638394, tenantId=1146029695717560320, journalId=1306274195778404443, issueId=1307086317918122434, language=CN, specialIssueTitle=, coverIllustrator=null, specialIssueEditor=, specialIssueAbout=)}, issueFiles=null, downloadFileDto=null}, startPage=304, endPage=315, ext={EN=ArticleExt(id=1307086912070644125, articleId=1307086910220956060, tenantId=1146029695717560320, journalId=1306274195778404443, language=EN, title=Evaporation-Induced Salt Precipitation in Soil-Groundwater System under Different Concentrations of NaCl : (Ⅰ) Physical Experiment, columnId=null, journalTitle=Northwestern Geology, columnName=null, runingTitle=null, highlight=null, articleAbstract=

Evaporation-induced salt precipitation in the soil-groundwater system is widespread in arid regions. However, there is no consensus on whether the temporal stage division of evaporation for saline water is consistent with that for pure water, which limits a deeper understanding of evaporation-induced salt precipitation in soil-groundwater system. To clarify the stage division and the controlling factors of evaporation-induced salt precipitation under different NaCl concentrations, indoor soil-column experiments were conducted using quartz sand as the porous medium. Five concentrations were tested: 0, 1, 3, 10, and 50 g/L NaCl. Two parallel replicates were performed for each concentration, giving a total of ten soil columns. The experiment lasted 43 days. Evaporation was recorded, air temperature, surface temperature and profile temperature were monitored, surface salt precipitation was documented, and the mass of the surface salt crust was measured. The results show that: ① The evaporation of pure water is consistent with previous studies and can be divided into three stages: Stage I, constant-rate or high-rate evaporation (days 1-18); Stage II, transitional or falling-rate evaporation (days 18-37); and Stage III, diffusion-limited or low-rate evaporation (days 37-43). ② Evaporation of saline water can also be divided into three stages, but the onset time and intensity of each stage vary with NaCl concentration. With increasing concentration, Stage I becomes shorter and Stage III starts earlier. For 1, 3, 10, and 50 g/L, Stage I lasted 17, 13, 7 and 4 days, respectively, and Stage III started on days 36, 31, 23 and 17, respectively. For moderate to high saline water (≥10 g/L), earlier development of a surface salt crust led to an earlier transition to Stage III and reduced cumulative evaporation. Using the mean cumulative evaporation of the two replicates, the values for 0, 1, 3, 10, and 50 g/L were 228.25, 131.92, 117.45, 109.53, and 29.16 cm, respectively. ③ The controlling factors vary with both concentration and evaporation stage: temperature potential dominated the early-stage evaporation for pure water, freshwater (1 g/L) and mildly saline water (3 g/L); during the transitional stage for moderately saline water (10 g/L), temperature potential and matric potential were both important, while solute potential became stronger and began to contribute to evaporation suppression; for highly saline water (50 g/L), solute potential dominated in the later stage.

, authors=Kaiying WEI, Jinting HUANG*, authorsList=Kaiying WEI, Jinting HUANG, authorCompany=null, correspAuthors=Jinting HUANG, authorNote=null, correspAuthorsNote=null, copyrightStatement=Copyright © 2026 Northwestern Geology. All rights reserved., copyrightOwner=null, extLink=null, articleAbsUrl=null, sourceXml=null, magXml=null, pdfUrl=null, pdf=null, pdfFileSize=null, pdfExtLink=null, richHtmlUrl=null, mobilePdfUrl=null, reviewReport=null, pdfFirstPage=null, abstractGraph=null, abstractGraphContent=null, abstractVideo=null, citation=null, cebUrl=null, magXmlContent=null, mapNumber=null, fund=null), CN=ArticleExt(id=1307086923076497914, articleId=1307086910220956060, tenantId=1146029695717560320, journalId=1306274195778404443, language=CN, title=不同浓度NaCl土壤–地下水蒸发积盐规律：（Ⅰ）物理实验, columnId=1307047819974570720, journalTitle=西北地质, columnName=非主题, runingTitle=null, highlight=null, articleAbstract=

土壤–地下水蒸发积盐在旱区广泛存在，但咸水与纯水的蒸发过程是否相同尚无统一认识，限制了人们对土壤–地下水蒸发积盐的深刻理解。为探明不同浓度NaCl的土壤–地下水蒸发积盐的阶段划分及其主控因素，本研究开展室内土柱实验，介质为石英砂，NaCl浓度分别为0 g/L、1 g/L、3 g/L、10 g/L、50 g/L，各浓度设两组平行实验，共10个土柱。实验历时43 d，记录蒸发量，监测气温、表面温度和剖面温度，记录表面积盐变化，并测定表面盐层质量。结果表明：①纯水蒸发过程与前人研究一致，划分为Ⅰ恒速/高速(1～18 d)、Ⅱ过渡/减速(18～37 d)、Ⅲ扩散/低速阶段（37～43 d）3个阶段。②咸水蒸发也可划分为3个阶段，但各阶段的起始时间与强度随NaCl浓度变化；浓度越大，第Ⅰ阶段持续时间越短，第Ⅲ阶段越早开始，浓度为1 g/L、3 g/L、10 g/L和50 g/L的盐水蒸发第Ⅰ阶段持续时间分别为17 d、13 d、7 d和4 d，第Ⅲ阶段开始时间分别是第36 d、31 d、23 d、17 d；中、重度咸水（≥10 g/L）因表层盐壳覆盖更早进入第Ⅲ阶段，导致累积蒸发量降低；两组平行实验的累积蒸发量取平均值，纯水、1 g/L、3 g/L、10 g/L和50 g/L分别为228.25 cm、131.92 cm、117.45 cm、109.53 cm、29.16 cm。③蒸发主控因子随浓度与蒸发阶段变化：纯水、淡水（1 g/L）、轻度咸水（3 g/L）蒸发早期受温度势主控；中度咸水（10 g/L）过渡期温度势与基质势并重，溶质势开始增强并参与抑制；重度咸水（50 g/L）后期以溶质势为主。

, authors=魏凯迎, 黄金廷*, authorsList=魏凯迎, 黄金廷, authorCompany=null, correspAuthors=黄金廷, authorNote=

魏凯迎（1999−），女，硕士生研究生，研究方向为水资源合理开发利用与生态保护。E−mail：

, correspAuthorsNote=
黄金廷（1979−），男，博士，教授，博士/硕士研究生导师，主要从事水资源合理开发利用与生态保护研究工作。E−mail：。
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魏凯迎（1999−），女，硕士生研究生，研究方向为水资源合理开发利用与生态保护。E−mail：

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魏凯迎（1999−），女，硕士生研究生，研究方向为水资源合理开发利用与生态保护。E−mail：

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a. A组不同浓度NaCl累积蒸发量随时间变化；b. B组不同浓度NaCl累积蒸发量随时间变化

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a. A组蒸发总累积量与NaCl浓度关系图；b. B组蒸发总累积量与NaCl浓度关系图

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a. A组不同浓度NaCl剖面土壤温度；b. B组不同浓度NaCl剖面土壤温度

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Experiment identifiers to different different concentrations of NaCl

, figureFileSmall=null, figureFileBig=null, tableContent=
NaCl溶液浓度纯水1 g/L3 g/L10 g/L50 g/L
盐度分类淡水淡水轻度咸水中度咸水重度咸水
A组A5A4A3A2A1
B组B5B4B3B2B1
), ArticleFig(id=1307087032455553421, tenantId=1146029695717560320, journalId=1306274195778404443, articleId=1307086910220956060, language=CN, label=表1, caption=

不同浓度NaCl组对应的实验编号

, figureFileSmall=null, figureFileBig=null, tableContent=
NaCl溶液浓度纯水1 g/L3 g/L10 g/L50 g/L
盐度分类淡水淡水轻度咸水中度咸水重度咸水
A组A5A4A3A2A1
B组B5B4B3B2B1
), ArticleFig(id=1307087032539439502, tenantId=1146029695717560320, journalId=1306274195778404443, articleId=1307086910220956060, language=EN, label=Tab.2, caption=

Salt precipitation process of the groups A and B

, figureFileSmall=null, figureFileBig=null, tableContent=
NaCl溶液
浓度		A组B组
盐斑析出时间盐分累积过程盐壳形成过程盐斑析出时间盐分累积过程盐壳形成过程
50 g/L
8 h8～72 h（3 d）72～1032 h4 h4～24 h（1 d）24～1032 h
10 g/L
12 h12～336 h（14 d）336～1032 h8 h8～192 h（8 d）192～1032 h
3 g/L
20 h20～528 h（22 d）528～1032 h10 h10～384 h（16 d）384～1032 h
1 g/L
48 h48～1032 h10 h10～408 h（17 d）408～1032 h
), ArticleFig(id=1307087032640102799, tenantId=1146029695717560320, journalId=1306274195778404443, articleId=1307086910220956060, language=CN, label=表2, caption=

A、B两组盐分析出过程

, figureFileSmall=null, figureFileBig=null, tableContent=
NaCl溶液
浓度		A组B组
盐斑析出时间盐分累积过程盐壳形成过程盐斑析出时间盐分累积过程盐壳形成过程
50 g/L
8 h8～72 h（3 d）72～1032 h4 h4～24 h（1 d）24～1032 h
10 g/L
12 h12～336 h（14 d）336～1032 h8 h8～192 h（8 d）192～1032 h
3 g/L
20 h20～528 h（22 d）528～1032 h10 h10～384 h（16 d）384～1032 h
1 g/L
48 h48～1032 h10 h10～408 h（17 d）408～1032 h
), ArticleFig(id=1307087032874983824, tenantId=1146029695717560320, journalId=1306274195778404443, articleId=1307086910220956060, language=EN, label=Tab.3, caption=

Evaporation metrics for groups A and B under different concentrations of NaCl

, figureFileSmall=null, figureFileBig=null, tableContent=
NaCl溶液浓度 （g/L）阶段I时长（d）A：阶段I平均蒸发速率（cm/d）B：阶段I平均蒸发速率（cm/d）A：阶段I累积（cm）B：阶段I累积（cm）A：1～43 d总累积（cm）B：1～43 d总累积（cm）A：阶段I占比（%）B：阶段I占比（%）
1174.264.9972.4084.73124.30139.5358.2460.72
3134.344.5756.4659.45119.52115.3947.2451.52
1076.216.0743.4742.48116.82102.2437.2141.55
5042.572.6110.2710.4226.0032.3239.5032.25
), ArticleFig(id=1307087032950481297, tenantId=1146029695717560320, journalId=1306274195778404443, articleId=1307086910220956060, language=CN, label=表3, caption=

不同浓度NaCl 两组阶段Ⅰ平均蒸发速率与累积蒸发量

, figureFileSmall=null, figureFileBig=null, tableContent=
NaCl溶液浓度 （g/L）阶段I时长（d）A：阶段I平均蒸发速率（cm/d）B：阶段I平均蒸发速率（cm/d）A：阶段I累积（cm）B：阶段I累积（cm）A：1～43 d总累积（cm）B：1～43 d总累积（cm）A：阶段I占比（%）B：阶段I占比（%）
1174.264.9972.4084.73124.30139.5358.2460.72
3134.344.5756.4659.45119.52115.3947.2451.52
1076.216.0743.4742.48116.82102.2437.2141.55
5042.572.6110.2710.4226.0032.3239.5032.25
), ArticleFig(id=1307087033025978770, tenantId=1146029695717560320, journalId=1306274195778404443, articleId=1307086910220956060, language=EN, label=Tab.4, caption=

Evaporation-stage for different concentrations of NaCl

, figureFileSmall=null, figureFileBig=null, tableContent=
NaCl溶液浓度纯水1 g/L3 g/L10 g/L50 g/L
第Ⅰ阶段0～18 d0～17 d0～13 d0～7 d0～4 d
第Ⅱ阶段18～37 d17～36 d13～31 d7～23 d4～17 d
第Ⅲ阶段37～43 d36～43 d31～43 d23～43 d17～43 d
), ArticleFig(id=1307087033298608531, tenantId=1146029695717560320, journalId=1306274195778404443, articleId=1307086910220956060, language=CN, label=表4, caption=

不同浓度NaCl蒸发阶段时间划分表

, figureFileSmall=null, figureFileBig=null, tableContent=
NaCl溶液浓度纯水1 g/L3 g/L10 g/L50 g/L
第Ⅰ阶段0～18 d0～17 d0～13 d0～7 d0～4 d
第Ⅱ阶段18～37 d17～36 d13～31 d7～23 d4～17 d
第Ⅲ阶段37～43 d36～43 d31～43 d23～43 d17～43 d
), ArticleFig(id=1307087033365717396, tenantId=1146029695717560320, journalId=1306274195778404443, articleId=1307086910220956060, language=EN, label=Tab.5, caption=

Correlation analysis between temperature and evaporation rate

, figureFileSmall=null, figureFileBig=null, tableContent=
NaCl浓度阶段A组B组
R2p 值是否通过显著性检验R2p 值是否通过显著性检验
纯水Ⅰ0.8605.3e-10是0.5261.3e-04是
Ⅱ0.3520.015是0.2600.044是
Ⅲ0.0130.806否0.1450.400否
1 g/LⅠ0.3430.035是0.1320.222否
Ⅱ0.4711.5e-04是0.0370.359否
Ⅲ0.1040.481否0.0000.979否
3 g/LⅠ0.1850.085否0.4350.004是
Ⅱ0.0610.441否0.1710.182否
Ⅲ0.4920.002是0.0980.238否
10 g/LⅠ0.0120.777否0.2150.209否
Ⅱ0.5813.7e-05是0.4615.1e-04是
Ⅲ0.0140.685否0.0120.705否
50 g/LⅠ0.7960.003是0.2610.196否
Ⅱ0.1040.155否0.0490.333否
Ⅲ0.2540.047是0.2990.028是
), ArticleFig(id=1307087033437020565, tenantId=1146029695717560320, journalId=1306274195778404443, articleId=1307086910220956060, language=CN, label=表5, caption=

温度与蒸发速率相关性分析表

, figureFileSmall=null, figureFileBig=null, tableContent=
NaCl浓度阶段A组B组
R2p 值是否通过显著性检验R2p 值是否通过显著性检验
纯水Ⅰ0.8605.3e-10是0.5261.3e-04是
Ⅱ0.3520.015是0.2600.044是
Ⅲ0.0130.806否0.1450.400否
1 g/LⅠ0.3430.035是0.1320.222否
Ⅱ0.4711.5e-04是0.0370.359否
Ⅲ0.1040.481否0.0000.979否
3 g/LⅠ0.1850.085否0.4350.004是
Ⅱ0.0610.441否0.1710.182否
Ⅲ0.4920.002是0.0980.238否
10 g/LⅠ0.0120.777否0.2150.209否
Ⅱ0.5813.7e-05是0.4615.1e-04是
Ⅲ0.0140.685否0.0120.705否
50 g/LⅠ0.7960.003是0.2610.196否
Ⅱ0.1040.155否0.0490.333否
Ⅲ0.2540.047是0.2990.028是
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不同浓度NaCl土壤–地下水蒸发积盐规律：（Ⅰ）物理实验
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魏凯迎 , 黄金廷 *
西北地质 | 非主题 2026,59(2): 304-315
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西北地质 |非主题 2026 , 59 (2) : 304 -315
不同浓度NaCl土壤–地下水蒸发积盐规律：（Ⅰ）物理实验
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魏凯迎（1999−），女，硕士生研究生，研究方向为水资源合理开发利用与生态保护。E−mail：

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魏凯迎 , 黄金廷*
作者信息
  • 西安科技大学地质与环境学院，陕西 西安　710054
通讯作者:
黄金廷（1979−），男，博士，教授，博士/硕士研究生导师，主要从事水资源合理开发利用与生态保护研究工作。E−mail：。
作者简介:

魏凯迎（1999−），女，硕士生研究生，研究方向为水资源合理开发利用与生态保护。E−mail：

Evaporation-Induced Salt Precipitation in Soil-Groundwater System under Different Concentrations of NaCl : (Ⅰ) Physical Experiment
Kaiying WEI , Jinting HUANG*
Affiliations
  • School of Geology and Environment, Xi’an University of Science and Technology, Xi’an 710054, Shaanxi, China
出版时间: 2026-04-20 doi: 10.12401/j.nwg.2025171
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土壤–地下水蒸发积盐在旱区广泛存在，但咸水与纯水的蒸发过程是否相同尚无统一认识，限制了人们对土壤–地下水蒸发积盐的深刻理解。为探明不同浓度NaCl的土壤–地下水蒸发积盐的阶段划分及其主控因素，本研究开展室内土柱实验，介质为石英砂，NaCl浓度分别为0 g/L、1 g/L、3 g/L、10 g/L、50 g/L，各浓度设两组平行实验，共10个土柱。实验历时43 d，记录蒸发量，监测气温、表面温度和剖面温度，记录表面积盐变化，并测定表面盐层质量。结果表明：①纯水蒸发过程与前人研究一致，划分为Ⅰ恒速/高速(1～18 d)、Ⅱ过渡/减速(18～37 d)、Ⅲ扩散/低速阶段（37～43 d）3个阶段。②咸水蒸发也可划分为3个阶段，但各阶段的起始时间与强度随NaCl浓度变化；浓度越大，第Ⅰ阶段持续时间越短，第Ⅲ阶段越早开始，浓度为1 g/L、3 g/L、10 g/L和50 g/L的盐水蒸发第Ⅰ阶段持续时间分别为17 d、13 d、7 d和4 d，第Ⅲ阶段开始时间分别是第36 d、31 d、23 d、17 d；中、重度咸水（≥10 g/L）因表层盐壳覆盖更早进入第Ⅲ阶段，导致累积蒸发量降低；两组平行实验的累积蒸发量取平均值，纯水、1 g/L、3 g/L、10 g/L和50 g/L分别为228.25 cm、131.92 cm、117.45 cm、109.53 cm、29.16 cm。③蒸发主控因子随浓度与蒸发阶段变化：纯水、淡水（1 g/L）、轻度咸水（3 g/L）蒸发早期受温度势主控；中度咸水（10 g/L）过渡期温度势与基质势并重，溶质势开始增强并参与抑制；重度咸水（50 g/L）后期以溶质势为主。

土壤盐渍化  /  水–热–溶质运移  /  土柱实验  /  蒸发积盐

Evaporation-induced salt precipitation in the soil-groundwater system is widespread in arid regions. However, there is no consensus on whether the temporal stage division of evaporation for saline water is consistent with that for pure water, which limits a deeper understanding of evaporation-induced salt precipitation in soil-groundwater system. To clarify the stage division and the controlling factors of evaporation-induced salt precipitation under different NaCl concentrations, indoor soil-column experiments were conducted using quartz sand as the porous medium. Five concentrations were tested: 0, 1, 3, 10, and 50 g/L NaCl. Two parallel replicates were performed for each concentration, giving a total of ten soil columns. The experiment lasted 43 days. Evaporation was recorded, air temperature, surface temperature and profile temperature were monitored, surface salt precipitation was documented, and the mass of the surface salt crust was measured. The results show that: ① The evaporation of pure water is consistent with previous studies and can be divided into three stages: Stage I, constant-rate or high-rate evaporation (days 1-18); Stage II, transitional or falling-rate evaporation (days 18-37); and Stage III, diffusion-limited or low-rate evaporation (days 37-43). ② Evaporation of saline water can also be divided into three stages, but the onset time and intensity of each stage vary with NaCl concentration. With increasing concentration, Stage I becomes shorter and Stage III starts earlier. For 1, 3, 10, and 50 g/L, Stage I lasted 17, 13, 7 and 4 days, respectively, and Stage III started on days 36, 31, 23 and 17, respectively. For moderate to high saline water (≥10 g/L), earlier development of a surface salt crust led to an earlier transition to Stage III and reduced cumulative evaporation. Using the mean cumulative evaporation of the two replicates, the values for 0, 1, 3, 10, and 50 g/L were 228.25, 131.92, 117.45, 109.53, and 29.16 cm, respectively. ③ The controlling factors vary with both concentration and evaporation stage: temperature potential dominated the early-stage evaporation for pure water, freshwater (1 g/L) and mildly saline water (3 g/L); during the transitional stage for moderately saline water (10 g/L), temperature potential and matric potential were both important, while solute potential became stronger and began to contribute to evaporation suppression; for highly saline water (50 g/L), solute potential dominated in the later stage.

soil salinization  /  water-heat-solute transport  /  soil column experiment  /  evaporation-induced salt precipitation
魏凯迎, 黄金廷. 不同浓度NaCl土壤–地下水蒸发积盐规律：（Ⅰ）物理实验. 西北地质, 2026 , 59 (2) : 304 -315 . DOI: 10.12401/j.nwg.2025171
Kaiying WEI, Jinting HUANG. Evaporation-Induced Salt Precipitation in Soil-Groundwater System under Different Concentrations of NaCl : (Ⅰ) Physical Experiment[J]. Northwestern Geology, 2026 , 59 (2) : 304 -315 . DOI: 10.12401/j.nwg.2025171
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最新遥感监测数据显示，中国盐渍化土壤总面积达36万km2，其中干旱区占比达69.03%，且呈现年均1.47%的增加速率（杨真等，2015；杨劲松等，2022）。土壤盐渍化作为全球性问题，其形成与蒸发驱动的水盐运移密切相关（王文科等，2018；Joseph et al.，2020；赵作章等，2023；Jannesarahmadi et al.，2024）。
现有研究表明，纯水蒸发过程可划分为3个阶段：①恒速/高速阶段（Ⅰ），表层湿润、蒸发受大气需水量控制；②过渡/减速阶段（Ⅱ），表层干化、毛细水补给受限，速率下降；③扩散/低速受限阶段（Ⅲ），表层干枯、蒸发受气相扩散或薄层传质控制（Lehmann et al.，2008；Shokri et al.，2011；唐朝生等，2011；Or et al.，2013；Han et al.，2013；Mosthaf et al.，2014；林宗泽等，2021；贾振江等，2023）。咸水蒸发因积盐与盐壳形态演化，导致阶段划分出现不同情况，多数学者用3个阶段来描述（Nachshon et al.，2011；Dong et al.，2021；唐洋等，2022；Zhang et al.，2023；周凤玺等，2024），但也有学者将其划分为4个或更多阶段（Li et al.，2021；刘世元，2024；靳芳等，2024；Jannesarahmadi et al.，2024），可见咸水蒸发阶段的划分尚无统一定论。
土壤–地下水咸水蒸发主要受离子组分与浓度、地下水埋深、介质性质和大气需水能力等多因素影响（袁磊等，2021）。前人研究表明：离子组分与浓度决定析盐矿物类型，改变盐壳孔隙结构，影响蒸发通量与阶段转换（张建国等，2019；付小磊等，2021；Xu et al.，2022；杨彩霞等，2023）；地下水埋深影响毛细上升高度能否到达蒸发面，埋深增大时基质势与浓度梯度减弱，表层积盐减少（李麒麟等，2003；王文科等，2021）；介质性质（粒径级配、孔径分布、润湿性）影响液相连通性与干层形成，从而改变各阶段的持续时间与强度（Wang et al.，2024）；大气需水能力由辐射与温湿度共同决定，湿润区蒸发力弱不利于持续积盐，干旱区蒸发力强则促进盐壳形成与维持（冯浩轩等，2025）。然而，现有研究对咸水蒸发过程中主控因子随浓度与阶段变化的规律分析略显不足。
为探究不同浓度NaCl下土壤−地下水的蒸发积盐规律，本研究设置了0、1 g/L、3 g/L、10 g/L、50 g/L等5个浓度NaCl，通过室内土柱实验，开展以下研究工作：①验证纯水蒸发阶段是否与前人研究的3个阶段相符合；②探究咸水蒸发与纯水蒸发阶段划分的异同；③探讨咸水蒸发特征及不同浓度、不同蒸发阶段的主导影响因素。研究成果可为NaCl型土体中水盐运移机理的分析提供参考依据。
1　材料与方法
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1.1　实验材料与制样
为避免天然土壤中颗粒级配不均和有机质等因素的干扰，选择均质黑色石英砂作为实验材料，粒径为0.35±0.05 mm，属细砂级配。实验溶液由NaCl与去离子水配制，据Robinove et al. （1958）盐度分类，采用0（纯水，对照组）、1 g/L、3 g/L、10 g/L、50 g/L NaCl溶液，分别代表淡水、轻度咸水、中度咸水和重度咸水开展实验研究，每种浓度设置两个平行土柱以保证规律一致性（表1）。实验土柱底部2 cm处铺设滤网，并分层填装石英砂，每层约3 cm，再用马氏瓶从底部供水至表面出现水膜，饱水半小时后排水，重复3次以保证石英砂均匀密实。填充完成后，调整恒定水位至距石英砂顶部表面下方6 cm，确保毛细上升高度达蒸发面（Lehmann et al.，2018）。
1.2　室内土柱实验装置
实验装置由马氏瓶、电子分析天平（生产厂家华志，型号PTQ-A+6，量程为6 kg，精度为0.01 g）、175 W卤光灯（生产厂家飞利浦，型号BR125，）和十个透明有机玻璃柱（内径为8 cm，高度为30 cm）组成。温度探头布设于滤网上方1、14、21 cm高度处（图1）。实验在室内开展，为减少侧壁热量交换，每个土柱的外壁包裹一层保温材料。
石英砂柱的质量变化数据由电子天平每隔5 min通过串口自动向电脑传输，表面温度数据则由测温仪（生产厂家奥思浦，型号ASP604A）每隔4 h手动记录，室内气温和湿度由实验室温湿度计（生产厂家妙昕，型号TH20R）自动记录，同时用数码相机（生产厂家FLIR；型号T630SC）记录表面盐斑发育情况。实验持续43 d，直到蒸发速率趋于稳定。实验结束后，刮取表面盐层后用电子天平称其质量。
1.3　数据处理
用Excel处理蒸发质量损失数据，计算蒸发速率与累积蒸发量，并使用Origin 2018绘图。将质量损失换算为等效蒸发水深，土柱内径为8 cm，对应截面积$ \begin{matrix}A\\ \end{matrix} $=50.27 cm2，按公式（1）计算。
$\Delta h=\dfrac{{m}_{{{t}_{1}}}-{m}_{{{t}_{2}}}}{{\rho }_{w}A} $
式中：$ \Delta h $为一定时间间隔内的蒸发水深，单位为cm；$ {\mathrm{m}}_{{{\mathrm{t}}_{1}}} $、$ {\mathrm{m}}_{{{\mathrm{t}}_{2}}} $分别为时刻$ {\mathrm{t}}_{1} $、$ {\mathrm{t}}_{2} $的土柱质量，单位为g；$ {\rho }_{w} $为水密度，取1 g/cm3。
蒸发速率计算公式如公式（2）所示。
$ E=\frac{\Delta h}{{t}_{2}-{t}_{1}}=\frac{{m}_{{{t}_{1}}}-{m}_{{{t}_{2}}}}{{\rho }_{w}A\left({t}_{2}-{t}_{1}\right)} $
式中：$ E $为蒸发速率，单位为cm/d；$ {t}_{2}-{t}_{1} $为时间间隔，单位为d。
累积蒸发量为各时间间隔蒸发水深损失的累加按公式（3）计算。
$ H\left(t\right)=\sum \limits_{i=1}^{n}\Delta {h}_{i}=\sum \limits_{i=1}^{n}\frac{{m}_{{{t}_{i-1}}}-{m}_{{{t}_{i}}}}{{\rho }_{w}A} $
式中：$ H(t) $为截止时刻$ t $的累积蒸发量，单位为cm。
2　实验结果分析
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2.1　不同浓度NaCl盐层的形成过程
A、B两组实验的50 g/L和10 g/L组均在12 h内出现明显盐斑（表2），A组3 g/L第20 h开始析盐，1 g/L第48 h出现细小盐斑；B组1、3g/L组均在10 h出现明显盐斑，且1 g/L比A组盐层形成得更完整，最终覆盖全表面。该差异可能因为实验所用的石英砂仅用纯净水冲洗而未进行灭菌处理，不排除存在少量有机质，从而导致盐斑出现时间与盐壳发育存在差别。经过43 d的持续蒸发，盐分向表层富集。实验结束后，50 g/L的两组盐层质量分别为18.25 g、19.56 g，10 g/L的两组盐层质量分别为6.82 g、7.83 g，3g/L的两组盐层质量分别为3.36 g、3.97 g，1 g/L的两组盐层质量分别为1.98 g、3.78 g。NaCl浓度越高，盐分析出越早，积盐现象越明显，实验结束后盐层质量越大且覆盖表面的比例也越大。
2.2　不同浓度NaCl土壤蒸发过程
A、B两组实验结果显示，纯水蒸发速率随时间变化可分为3个阶段（图2）。第Ⅰ阶段（恒速/高速阶段）持续18 d，在此期间两组平均蒸发速率最高，分别为6.35 cm/d、7.43 cm/d；第Ⅱ阶段（减速/过渡阶段）从18～37 d，平均蒸发速率下降至4.04 cm/d、4.69 cm/d并趋于稳定；第Ⅲ阶段（扩散/低速阶段）启动于37 d后，平均蒸发速率继续下降至3.25 cm/d、3.86 cm/d，并在末期基本不变。实验结束（第43 d），两组总累积蒸发量分别为210.51 cm、246.00 cm。纯水组蒸发速率和累积蒸发量均大于咸水蒸发。
咸水蒸发过程整体上也表现为3个阶段，但阶段长度与蒸发量随浓度变化。第Ⅰ阶段时长随浓度升高显著缩短（表3，图3）：由1 g/L的17 d、3 g/L的13 d，降至10 g/L的7 d与50 g/L的4 d。浓度越高，第Ⅰ阶段对总蒸发量的贡献比例越低，由58%～61%（1 g/L）、47%～52%（3 g/L）、37%～42%（10 g/L）下降至32%～40%（50 g/L）。到第43 d的累积蒸发量总体随浓度增加而降低（表3，图4）：50 g/L与10 g/L、3 g/L、1 g/L相比，A组累积蒸发量分别下降约77.74%、78.25%、79.09%，B组累积蒸发量分别下降约68.38%、71.99%、76.83%。实验结束时的累积蒸发量随NaCl浓度升高而降低，且符合对数拟合，R2达到0.94（图5）。A组10 g/L与3 g/L的累积蒸发量变化曲线接近，可能是由于实验全期10 g/L的表面温度均比3 g/L高，蒸发量较大。
2.3　不同浓度NaCl土柱温度变化
卤光灯持续加热使室温自初始30.5 ℃上升至第15天的42.5 ℃，随后波动下降，实验期内平均气温38.7 ℃。相对湿度平均36.2%（图6）。
根据各组盐壳覆盖时间（表2、表3）及不同浓度NaCl表面温度随时间变化图（图7）可知，覆盖后纯水组表面温度整体高于咸水组。盐壳覆盖后的表面温度均值为：50 g/L的A1、B1为81.8 ℃、86.0 ℃，10 g/L的A2、B2为82.1 ℃、77.5 ℃，3 g/L的A3、B3为72.0 ℃、92.7 ℃，1 g/L的A4、B4为97.1 ℃、87.8 ℃，纯水组的A5、B5为106.3 ℃、83.9 ℃。以1 g/L为参照，盐壳覆盖后10 g/L与50 g/L的表面温度分别降低12.7、8.6 ℃；以纯水为参照，分别降低15.3 ℃、11.2 ℃；3 g/L相对1 g/L也降低约10 ℃。B5（纯水）因实验开始前存在薄干层，盐壳覆盖前表面温度偏高，覆盖后回落到83.9 ℃，仍符合纯水高于咸水的总体规律。
以盐层覆盖前与覆盖后的稳定期对比，剖面土壤温度均呈上部高、下部低，且盐层覆盖后上下温差增大。试验开始第1天，各组柱内温差较小，整体接近等温。盐层覆盖前，21 cm与1 cm之间温差多为7～9 ℃；覆盖后稳定期，该温差增至10～13 ℃，分别为纯水9.93 ℃、1 g/L 11.62 ℃、3 g/L 12.87 ℃、10 g/L 11.04 ℃、50 g/L 11.44 ℃。覆盖后各组上部温度多稳定在57～63 ℃，下部温度在46～51 ℃范围内波动。其中，50 g/L组下部由约31 ℃升至约47 ℃，10 g/L组下部由约55 ℃降至49～51 ℃。总体来看，盐层覆盖后剖面垂向温差明显扩大（图8）。
3　讨论
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3.1　蒸发阶段时间划分
纯水蒸发过程可划分为3个阶段：初期为快速蒸发期，此时表层含水量大，蒸发受温度主导，质量损失率最高；随后进入过渡/减速期，表层逐渐干燥，蒸发速率由毛细输运与气相扩散共同决定，质量损失曲线缓慢下降并趋于平稳；最终进入扩散受限或低速期，毛细水分补给能力减弱，气相扩散成为主控过程，蒸发速率下降并保持在较低水平。纯水蒸发曲线在第18 天与第37天附近出现拐点，据此可划分3个阶段（图2）。因此，本研究验证了纯水蒸发过程的三阶段划分（Lehmann et al.，2008；唐朝生等，2011；Han et al.，2013；Mosthaf et al.，2014；林宗泽等，2021；贾振江等，2023）。
咸水蒸发也可分为3个阶段（表3、表4，图3、图4）。1 g/L组第Ⅰ阶段持续17 d，48 h出现盐斑，进入第Ⅱ阶段后蒸发速率下降缓慢，第Ⅲ阶段在36 d后开始；3 g/L组第Ⅰ阶段13 d，第20 h即出现盐斑，31 d进入第Ⅲ阶段；10 g/L组第Ⅰ阶段7 d，12 h内即析出盐晶，23 d进入第Ⅲ阶段。50 g/L组第Ⅰ阶段仅4 d，8 h内即出现大量盐析，表面迅速被盐层覆盖，17 d即进入第Ⅲ阶段。总体上，浓度越高，第Ⅰ阶段越短，第Ⅱ阶段越早开始，50 g/L组累积蒸发量显著低于1 g/L组，咸水组蒸发量低于纯水组。
3.2　土壤–地下水蒸发影响因素分析
3.2.1　盐壳对蒸发的影响
盐壳通过两个方面影响蒸发：①盐晶在表层堆积会堵塞孔隙，使土体内部水分向表面的补给变慢；②盐层覆盖会改变表面的受热情况。例如，反射增强、吸热减少，从而影响表面温度。第Ⅰ阶段内，咸水组早期的盐斑多为湿润状态，局部仍保持潮湿并参与蒸发，因此对蒸发速率的影响不明显。随着盐斑干燥形成盐层后覆盖在表面，表层孔隙与渗透性下降，毛细连通性降低，蒸发进入扩散控制阶段。此外，浓度越大，盐层覆盖后的表面温度越低（图7），纯水与1 g/L为95.1 ℃、92.5 ℃，而3 g/L、10 g/L、50 g/L仅82.4 ℃、81.8 ℃、80.9 ℃。此外，盐壳形成使剖面温差增大（图8），盐层覆盖后1～21 cm的温差在各浓度组普遍增大约13 ℃。
3.2.2　浓度对蒸发的影响
实验结果（表3，图2、图3、图4、图5）显示，浓度越高，表层达到饱和并析盐的时间越早，盐层越快覆盖整个表面，累积蒸发量越小。在轻度咸水（3 g/L）中，溶质势开始发挥影响，促使盐斑形成降低毛细上升通量；在中度咸水（10 g/L）中，溶质势与由此引起的孔隙与渗透性变化成为主要限制因子，蒸发速率降低；在重度咸水（50 g/L）中，溶质势占主导，蒸发快速进入扩散受限的低通量阶段。第Ⅲ阶段（扩散/低速），系统普遍转向以溶质势为主导，中、重度咸水（≥10 g/L，尤其50 g/L）因盐壳形成过快而较早丧失毛细连通，导致压力梯度迅速降低、毛细上升通量受限，蒸发被气相扩散控制，50 g/L的盐壳覆盖表面仅需1～3 d，第Ⅰ阶段仅4 d，B组至实验结束累积蒸发量仅1635 g。同时，低浓度组在前期完成的蒸发量占比更高，A、B组第Ⅰ阶段占比分别为58%和61%，10 g/L与50 g/L因为盐层形成更早，前期持续时间缩短，后期低速阶段所占比例增加。总体上，浓度越高，阶段转折点越早出现，累积蒸发量越小。
3.2.3　表面温度对蒸发的影响
温度是驱动蒸发的关键因素之一，按不同浓度的阶段划分（表4），对表面温度与蒸发速率进行了Pearson相关分析（表5）。结果显示：纯水、淡水（1 g/L）与轻度咸水（3 g/L）在第Ⅰ阶段普遍呈显著相关（多数组合p<0.05，R2较高）；随浓度升高，第Ⅰ阶段的R2和显著性下降，部分在第Ⅱ、Ⅲ阶段相关性减弱或不显著；50 g/L在多数阶段的R2最低、显著性弱。说明中、重度咸水的蒸发更早受盐壳与溶质势影响，质量变化对温度变化的响应减弱，从而使温度与质量的线性关联在后期不再显著。
3.2.4　主控因子判别与分级结果
为比较不同浓度的不同阶段下蒸发过程的主控因素，本文依据蒸发速率变化、同步监测的气温与土壤温度，以及表层盐壳的形成与覆盖过程，对影响蒸发的因素进行分级判别。将蒸发控制因素归纳为3类：①温度势，代表温度变化对蒸发的作用；②基质势，代表毛细力与吸附力对土壤水的作用，该作用随土体干燥和盐壳发育而减弱；③溶质势，代表浓度升高对水分蒸发的抑制作用，浓度越高该抑制越明显。分级方法采用0到3的主导性等级评价，3表示主导，2表示次要，1表示弱，0表示缺失。各浓度均设置A、B两组平行土柱，判别结果在两组之间保持一致性，用于降低偶然性影响并检验重复性。
不同浓度与阶段下温度势、基质势与溶质势的分级结果（图9）显示，蒸发主控因子随浓度与阶段发生变化。纯水、1 g/L与3 g/L在第I阶段以温度势为主控，基质势次要，溶质势较弱。第Ⅱ阶段纯水以基质势为主控，1 g/L仍以温度势为主，3 g/L溶质势开始增强并参与控制。第III阶段时，随着盐分累积，溶质势逐渐增强，3 g/L与10 g/L以溶质势为主控。10 g/L在阶段II表现为温度势与基质势并重，溶质势增强并抑制蒸发。50 g/L在3个阶段均以溶质势为主控因子。
4　结论
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（1）纯水蒸发过程与前人研究一致，可划分为：Ⅰ恒速/高速期（0～18 d）、Ⅱ过渡/减速期（18～37 d）、Ⅲ扩散/低速期（>37 d）3个阶段。
（2）咸水蒸发也可分为3阶段，但阶段持续时间和强度随浓度变化。浓度越高，第Ⅰ阶段持续时间越短，盐析出越早，盐壳更快形成，蒸发更早进入扩散受限期，累积蒸发量越少。1g/L、3g/L、10g/L、50 g/L的第Ⅰ阶段为17 d、13d、7d、4 d，A组累积蒸发量由111.81 cm降至26.00 cm。
（3）蒸发主控因子随蒸发阶段与浓度而变化：纯水、淡水与轻度咸水/第Ⅰ阶段以温度势为主，中度咸水/第Ⅱ阶段温度、基质势、溶质势共同作用，重度咸水/第Ⅲ阶段以溶质势为主。纯水与轻度咸水（1 g/L、3 g/L）第Ⅰ阶段温度与蒸发速率通过显著性检验后R2较高，纯水R2达到0.86，10 g/L、50g/L的R2降低，显著性弱。

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2026年第59卷第2期
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doi: 10.12401/j.nwg.2025171
  • 接收时间：2026-01-20
  • 首发时间：2026-09-16
  • 出版时间：2026-04-20
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  • 收稿日期：2026-01-20
  • 修回日期：2026-02-05
  • 录用日期：2026-02-08
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    西安科技大学地质与环境学院，陕西 西安　710054

通讯作者:

黄金廷（1979−），男，博士，教授，博士/硕士研究生导师，主要从事水资源合理开发利用与生态保护研究工作。E−mail：。
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2种不同金属材料的力学参数
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Family		 属数
Number of
genus		 种数
Number of
species		 占总种数比例
Percentage of
total species (%)		 属
Genus		 种数
Number of
species		 占总种数比例
Percentage of total
species (%)
鹅膏菌科Amanitaceae 2 11 5.26 鹅膏菌属 Amanita 10 4.78
小菇科 Mycenaceae 2 12 5.74 丝盖伞属 Inocybe 5 2.39
多孔菌科 Polyporaceae 8 14 6.70 蜡蘑属 Laccaria 5 2.39
红菇科 Russulaceae 3 23 11.00 小皮伞属 Marasmius 6 2.87
小菇属 Mycena 11 5.26
光柄菇属 Pluteus 5 2.39
红菇属 Russula 17 8.13
栓菌属 Trametes 5 2.39
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