馮壯壯,史海濱,苗慶豐,孫 偉,劉美含,代麗萍
基于HYDRUS-1D模型的河套灌區(qū)典型夾砂層耕地水分利用分析
馮壯壯,史海濱※,苗慶豐,孫 偉,劉美含,代麗萍
(1. 內(nèi)蒙古農(nóng)業(yè)大學(xué)水利與土木建筑工程學(xué)院,呼和浩特 10018;2. 高效節(jié)水技術(shù)裝備與水土環(huán)境效應(yīng)內(nèi)蒙古自治區(qū)工程研究中心,呼和浩特 10018)
為研究夾砂層耕地水分利用規(guī)律,以河套灌區(qū)典型夾砂層土壤耕地為研究對(duì)象,利用在春玉米生育期田間監(jiān)測數(shù)據(jù),應(yīng)用土壤水分運(yùn)動(dòng)數(shù)值模型,探究對(duì)夾砂層土壤田間蒸散發(fā)、作物耗水及深層土壤水分的補(bǔ)給與深層滲漏規(guī)律。選擇2種土壤的夾砂層埋深梯度S1(40~95 cm)、S2(60~110 cm),設(shè)置了3個(gè)灌水水平W1(252.5 mm)、W2(315.85 mm)、W3(378.75 mm)開展田間試驗(yàn),同不含夾砂層處理B作對(duì)照,并應(yīng)用HYDRUS-1D模型模擬春玉米生育期田間蒸散發(fā),土壤水分深層滲漏及地下水補(bǔ)給耕層水量與根系吸水量,與不含夾砂層處理對(duì)比分析夾砂層對(duì)田間水分利用影響。結(jié)果表明:隨著砂層埋深增加,棵間蒸發(fā)損失減小,葉面蒸騰水量增加;不含夾砂層處理玉米田間毛管向上補(bǔ)給水量較淺埋砂層與深埋砂層處理分別大57.01%、118.53%,灌水量為315.85 mm時(shí)含夾砂層處理的土壤水分深層滲漏最?。挥衩咨趦?nèi)根系吸水量隨砂層埋深的增加而減少,不含夾砂層處理根系吸水量最大。淺埋砂層與深埋砂層處理分別為蒸散量的55.51%、61.31%,不含夾砂層處理為66.69%;暫時(shí)性虧缺水量從大到小依次為:S2、S1、B,水分從大到小依次為:B、S2、S1。綜合考慮夾砂層土壤水分遷移、作物水分利用規(guī)律,建議在夾砂層耕地春玉米灌溉根據(jù)砂層分布因地制宜定灌溉制度,當(dāng)夾砂層埋深在40~110 cm范圍時(shí),推薦春玉米在生育期灌溉定額為315.85 mm。該研究結(jié)果可為河套灌區(qū)含有夾砂層農(nóng)田灌溉制度的制定提供理論指導(dǎo)。
灌溉;土壤含水率;夾砂層土壤;土壤蒸散;地下水補(bǔ)給;深層滲漏;HYDRUS-1D模型
水資源短缺和土壤鹽堿化已成為限制河套灌區(qū)灌溉農(nóng)業(yè)可持續(xù)發(fā)展的重要問題[1],準(zhǔn)確評(píng)估灌區(qū)灌溉用水,對(duì)灌區(qū)農(nóng)業(yè)生產(chǎn)與水資源優(yōu)化利用意義重大[2]。關(guān)于非飽和帶土壤中水分動(dòng)態(tài)的研究,大多研究都集中于均質(zhì)土壤。而自然界中土壤剖面并非呈現(xiàn)簡單的均一分布,由于河流黏、砂交錯(cuò),黃河灌淤等[3]形成復(fù)雜多變的層狀土壤剖面結(jié)構(gòu)[4],土層夾砂結(jié)構(gòu)成為河套灌區(qū)常見的一種土體構(gòu)型[5]。已有研究表明,夾砂層與砂層粒徑都會(huì)對(duì)土壤水分入滲速率、入滲量產(chǎn)生影響,砂層越接近地面或砂層粒徑越大,越有利于土壤水分入滲[6]。砂層對(duì)水分蒸發(fā)的影響取決于砂層與土層導(dǎo)水率的大小,砂層對(duì)土壤表層鹽分的抑制率大于土層[7-8]。
由于土壤、作物、氣象、地下水、灌溉和管理的空間差異,水文過程變化復(fù)雜,農(nóng)田試驗(yàn)耗時(shí)費(fèi)力[9],確定有效灌溉策略更為便捷的替代方法是對(duì)影響灌溉策略土壤水平衡與作物生產(chǎn)力進(jìn)行建模[10]。HYDRUS-1D模型可以通過模擬多層變飽和土中的一維水運(yùn)動(dòng)對(duì)實(shí)際蒸散量和深層滲流進(jìn)行預(yù)測,Zhou等[11]通過HYDRUS-1D對(duì)作物生長季內(nèi)土壤水分蒸散量與深層滲漏量模擬結(jié)果表明田間蒸散與土壤水分深層滲漏是作物水分循環(huán)的主導(dǎo)過程,Hou等[1]應(yīng)用HYDRUS-1D對(duì)海流圖流域玉米水分利用模擬得出當(dāng)?shù)叵滤裆畛?57 cm時(shí),玉米就不能利用地下水進(jìn)行蒸騰。目前,含夾砂層土壤的水分分布及運(yùn)移規(guī)律的研究大多通過在室內(nèi)土柱試驗(yàn)或者數(shù)值模擬進(jìn)行,對(duì)于有實(shí)際作物種植和實(shí)際田間管理以及年內(nèi)氣候變化等條件耦合作用下的含夾砂層耕地研究較少。
本研究基于河套灌區(qū)典型夾砂層土壤田間觀測數(shù)據(jù),通過HYDRUS-1D軟件對(duì)不同夾砂層分布下的玉米農(nóng)田蒸散發(fā)、土壤水分深層滲漏與地下水補(bǔ)給、玉米根系吸水等過程進(jìn)行數(shù)值模擬與分析,研究了典型夾砂層耕地間水分利用與轉(zhuǎn)化規(guī)律,以期為當(dāng)?shù)剡M(jìn)一步制定農(nóng)田灌溉用水策略、有效提高灌溉水利用率提供理論依據(jù)。
1.1 試驗(yàn)區(qū)概況
試驗(yàn)區(qū)設(shè)在內(nèi)蒙古河套灌區(qū)中部巴彥淖爾市曙光試驗(yàn)站,位于東經(jīng)107o13′23″,北緯40o43′26″。所在地區(qū)屬溫帶大陸性干旱-半干旱氣候區(qū),氣候干燥、降水稀少、蒸發(fā)強(qiáng)烈、冬季漫長寒冷。多年平均降水量為133.90 mm,多年平均氣溫為8.64 ℃,多年作物生育期平均氣溫為19.11 ℃。試驗(yàn)地土壤屬于黃河灌淤土,具有典型夾砂結(jié)構(gòu),地下水平均埋深約為2.4~2.9 m,地下水礦化度為1.108 g/L。2020年試驗(yàn)區(qū)生育期內(nèi)降雨量、潛在作物蒸散量、地下水埋深如圖1所示。
供試作物為春玉米,品種為“西蒙3358”,采用寬窄行種植,寬窄行距分別為60、40 cm。試驗(yàn)田間管理參照當(dāng)?shù)剞r(nóng)業(yè)生產(chǎn)方式進(jìn)行。為研究土壤夾砂層分布對(duì)玉米田間土壤水分運(yùn)移分布影響及玉米生長對(duì)不同夾砂層土壤水分的響應(yīng),參照當(dāng)?shù)氐墓嗨O(shè)置了3個(gè)灌水水平W1(252.5 mm)、W2(315.85 mm)、W3(378.75 mm),兩個(gè)夾砂層埋深梯度處理(S1、S2),砂層埋深較淺為S1(40~95 cm),砂層埋深較深為S2(60~110 cm),同時(shí)設(shè)置與夾砂層處理灌水相同的3個(gè)不含夾砂層的處理BW1、BW2、BW3。各處理灌水量及灌水時(shí)間詳見表1。其中不同夾砂層處理與不含夾砂結(jié)構(gòu)土壤處理均在試驗(yàn)區(qū)內(nèi)選取,在試驗(yàn)布置前期,通過土鉆鉆孔法確定試驗(yàn)區(qū)砂層的空間分布,選定有代表性砂層分布的夾砂層耕地作為試驗(yàn)地布置試驗(yàn),由表1知,夾砂層埋深與厚度存在由取樣誤差造成的差異,為減小取樣誤差對(duì)模擬的影響,在HYDRUS -1D模型中劃分統(tǒng)一的砂層埋深與厚度(S1砂層埋深均設(shè)置為40 cm,厚度均設(shè)置為55 cm;S2砂層埋深均設(shè)置為60 cm,厚度均設(shè)置為50 cm)。每個(gè)處理小區(qū)面積為48 m2,長寬比為3∶1。試驗(yàn)在玉米生育期內(nèi)進(jìn)行,播種時(shí)間為2020年5月4日,收獲時(shí)間為2020年9月25日。
1.3.1 氣象與含水率、土壤基質(zhì)勢
氣象數(shù)據(jù)通過試驗(yàn)站自動(dòng)氣象站(HOBO H21-001,Onset,USA)獲取,包括最高氣溫、最低氣溫、相對(duì)濕度、風(fēng)速、太陽輻射、氣壓、降水量等。地下水位由觀測井觀測。土壤體積含水率由TRIME-TDR 型時(shí)域反射儀(IMKO GmbH,Ettlingen,德國)測定。使用土壤張力計(jì)對(duì)土壤的基質(zhì)勢進(jìn)行觀測,負(fù)壓計(jì)(張力計(jì))在砂層的上下部分別埋設(shè),張力計(jì)及TRIME管埋設(shè)如圖2所示,典型夾砂層耕地土壤物理性質(zhì)如表2所示。玉米生育期具體時(shí)段[12]如表3所示。
表1 不同處理的灌水日期及灌水量
表2 典型夾砂層土壤物理特性
表3 玉米生育期劃分
1.3.2 玉米葉面積指數(shù)
玉米生育期內(nèi)第20~30天記錄玉米株高,分別測量葉片的長度與葉片的最寬寬度計(jì)算單株玉米總?cè)~面積LA,計(jì)算公式[13]如下:
式中L為第片葉片的長度,cm;W為第片葉片的寬度,cm;為玉米株數(shù);LA為單株玉米總?cè)~面積,cm2;0.75為回歸系數(shù)。
玉米葉面積指數(shù)計(jì)算公式為
式中LAI為葉面積指數(shù);I為株距,cm;R為行距,cm。
1.3.3 棵間蒸發(fā)量
棵間土壤蒸發(fā)量通過布置在各處理的自制微型土壤蒸發(fā)桶測定。該裝置由PVC管制成,分為內(nèi)筒與外桶兩個(gè)部分,管內(nèi)徑分別為110、125 mm。每日17時(shí)使用精度為0.01 g的電子秤稱取蒸發(fā)桶質(zhì)量,為保證準(zhǔn)確性,除了灌水與降雨后換土外,保持每3 d換1次土的頻率。
1.3.4 土壤水分特征曲線
土壤水分特征曲線由壓力薄膜儀測定。首先將土樣浸泡在蒸餾水中至飽和,稱質(zhì)量后放入1500F1型壓力薄膜儀(1500F1 Extractor,SoilMoisture,美國)中,對(duì)土樣施加一定的壓力,迫使土壤水分滲出,達(dá)到平衡時(shí),土壤基質(zhì)勢與所加壓力值相等,測量此時(shí)土壤含水率,標(biāo)定土壤的水分特征曲線。
應(yīng)用EXCEL2016軟件進(jìn)行數(shù)據(jù)整理,Origin2018軟件對(duì)本文中的插圖進(jìn)行繪制,DPS(7.05)數(shù)據(jù)處理系統(tǒng)做顯著性差異分析,HYDRUS-1D軟件建立模型模擬。
1.5.1 HYDRUS-1D水分運(yùn)動(dòng)方程
HYDRUS-1D模型[14-15]基于Richards方程,模擬多層變飽和土壤中的一維水分運(yùn)動(dòng),用于預(yù)測深層滲漏、補(bǔ)給與蒸散量。其數(shù)學(xué)模型描述如下:
式中為體積含水率,cm3/cm3;為時(shí)間,d;為非飽和導(dǎo)水率,cm/d;為基質(zhì)勢,cm;為垂直坐標(biāo),cm(假設(shè)地表為0,向下為正);()為根系吸水源匯項(xiàng),cm/d。
1.5.2 根系吸水速率
采用Feddes模型計(jì)算根系吸水速率,計(jì)算公式[16]為
式中()為水分脅迫反應(yīng)函數(shù);()為標(biāo)準(zhǔn)化的根系吸水分布函數(shù);p為作物潛在蒸騰速率,cm/d。
Feddes模型參數(shù)采用HYDRUS-1D模型系統(tǒng)所提供的參數(shù)[14]。根系吸水厭氧點(diǎn)土壤基質(zhì)勢P0為-10 cm,根系吸水最適點(diǎn)開始時(shí)土壤基質(zhì)勢P0pt為-25 cm,根系吸水最適點(diǎn)結(jié)束時(shí)土壤基質(zhì)勢P2H、P2L分別為-500、-500 cm,凋萎點(diǎn)對(duì)應(yīng)土壤基質(zhì)勢P3為-24 000 cm,兩個(gè)假設(shè)的潛在作物蒸騰速率r2H、r2L分別為0.5、0.1 cm/d。
1.5.3 葉面蒸騰與土壤蒸發(fā)計(jì)算
參考作物蒸散量ET0由FAO推薦的Penman-Monteith公式[17]計(jì)算,由于玉米覆蓋土壤表面,因此被劃分為潛在蒸發(fā)量p(mm)與潛在蒸騰量p(mm)。公式如下:
式中為冠層輻射消光系數(shù),本文取0.463[18];ETc為作物實(shí)際蒸散發(fā),mm;c為作物系數(shù),不同生育期取值分別為:苗期至拔節(jié)期0.7、拔節(jié)期至灌漿期1.2、灌漿期至成熟期0.6[17]。
1.5.4 模型參數(shù)率定與檢驗(yàn)
模擬范圍為耕層深度,為地面以下120 cm,垂向離散為121個(gè)節(jié)點(diǎn),離散單元為cm,時(shí)間離散單元為d。模擬時(shí)段為玉米作物生育期(5月4日—9月25日),共145 d。對(duì)土層與砂層的土壤水力參數(shù)進(jìn)行了校準(zhǔn)和驗(yàn)證,如表4所示。
通過決定系數(shù)(2)、均方根誤差(Root Mean Square Error,RMSE)和納什效率系數(shù)(Nash-Sutcliffe Efficiency coefficient,NSE)對(duì)模型模擬效果進(jìn)行評(píng)價(jià),其中NSE越接近1,表示模型模擬精度越高。
表4 不同處理下各土層土壤水力特征參數(shù)
注:r為土壤殘余含水率,s為土壤飽和含水率,cm3·cm-3;、、為相對(duì)經(jīng)驗(yàn)參數(shù),一般為0.5;s為飽和導(dǎo)水率,cm·d-1。
Note:ris residual water content andsis saturated water content, cm3·cm-3;,, andare relative empirical parameters, andis generally 0.5;sis saturated hydraulic conductivity, cm·d-1.
受玉米生育期內(nèi)氣溫變化與土壤質(zhì)地影響[19],試驗(yàn)區(qū)玉米在生育期內(nèi)不同處理的蒸騰量大于根系吸水量,產(chǎn)生了不同程度的暫時(shí)性水分虧缺。暫時(shí)性水分虧缺會(huì)造成玉米葉片暫時(shí)性萎蔫,在玉米關(guān)鍵生育期內(nèi)出現(xiàn)水分虧缺還會(huì)影響玉米籽粒的形成與生長發(fā)育。暫時(shí)性水分虧缺水量計(jì)算公式為
式中WD為暫時(shí)性虧缺水量,mm;為根系吸水量,mm。
玉米水分生產(chǎn)力公式[20]為
式中w為水分生產(chǎn)力,kg/(hm2·mm);Yield為玉米產(chǎn)量,kg/hm2;為灌溉水量,mm;為降雨量,mm。
使用2020年6月7日—9月16日測量的土壤含水率對(duì)模型水力參數(shù)進(jìn)行了率定,選取其中S1W2處理水分率定過程繪圖,利用均方根誤差RMSE和決定系數(shù)2、納什效率系數(shù)NSE評(píng)估模型精度。土壤含水率模擬值與觀測值的精度驗(yàn)證如圖3所示。利用具有代表性的4組實(shí)測土壤基質(zhì)勢與土壤水分特征曲線對(duì)模型生育期土壤水分模擬進(jìn)行間接驗(yàn)證[21],見圖4和圖5。結(jié)果表明模型模擬精度較高,土壤含水率模型計(jì)算值與實(shí)測值的決定系數(shù)2、NSE值均約為0.9,RMSE均較小,土壤基質(zhì)勢與土壤水分特征曲線模擬值2均在0.7以上,表明HYDRUS-1D模擬含有夾砂層土壤水分運(yùn)動(dòng)有較好的適用性。同時(shí),由于夾砂層土壤結(jié)構(gòu)較為復(fù)雜,當(dāng)土壤含水率較小時(shí),TRIME管與土壤接觸不緊密,造成測得如圖3所示土壤含水率為0的情況出現(xiàn)[22],率定后的土壤水力參數(shù)如表4所示。
通過HYDRUS-1D模擬得出,玉米田間葉面蒸騰與棵間蒸發(fā)速率隨玉米生長發(fā)育與田間微氣候改變,最大蒸騰蒸散速率都發(fā)生在灌漿期間,玉米生育期棵間蒸發(fā)a與p分布如圖6所示,最大土壤蒸發(fā)速率在玉米苗期與拔節(jié)期之間,是因?yàn)槊缙谂c拔節(jié)期玉米的株高與葉面積較小,使得地表植被覆蓋率較小,玉米株高葉面積如圖7所示,在玉米拔節(jié)期前,砂層深埋(S2)處理的葉面積指數(shù)較砂層淺埋(S1)處理更大,不含砂層(B)處理與S2處理的葉面積指數(shù)較為接近。如圖8所示,在3個(gè)灌水水平W1、W2、W3條件下,玉米全生育期內(nèi),S2處理較S1處理的ETp分別增加8.74%、8.97%、7.29%,p減小14.76%、8.59%、19.06%,a分別減小8.30%、8.32%、16.93%,p分別增加了13.40%、12.36%、2.24%,B處理較S1處理p分別減小35.99%、56.55%、6.37%,p分別增加24.32%、10.19%、2.48%。隨著灌水量的增加,各夾砂層處理p均減小,p均增加,而不含夾砂層處理在不同灌水量下p與p變化較小,沒有表現(xiàn)出明顯增減趨勢。不同處理ETP和p均表現(xiàn)為B處理最大,S2處理次之,S1處理最小,p則呈現(xiàn)出相反的規(guī)律,其中S2處理較S1處理棵間土壤蒸發(fā)損失水量減小13.60%。結(jié)果顯示,土壤質(zhì)地與灌水量共同對(duì)田間蒸散發(fā)變化與分配產(chǎn)生影響[23],隨灌水量增加,田間ETp總體增大,向p分配更多,而當(dāng)砂層淺埋時(shí)玉米蒸騰水分利用少,蒸發(fā)損失多。
利用HYDRUS-1D模擬土壤水分通量,通過試驗(yàn)觀測的土壤體積含水率與土壤深度的乘積可得到當(dāng)前土層深度的土壤貯水量,結(jié)果見圖9。通過分析主要根系層分布深度(0~40 cm)與耕層底部120 cm處土壤水分通量,探討不同夾砂層分布與不同灌水量處理下的主要根系區(qū)、耕層水分補(bǔ)給與深層滲漏規(guī)律。當(dāng)上層土壤含水率較小時(shí),由于水勢差驅(qū)動(dòng),深層土壤水分通過上升毛管水運(yùn)動(dòng),會(huì)向上層土壤補(bǔ)給[24],當(dāng)灌水或者降雨的水量超過土層所能持蓄的最大水量時(shí)[25-26],會(huì)導(dǎo)致土壤水分向深層滲漏。
在40和120 cm深度處,砂層淺埋(S1)處理玉米生育期土壤水分向上層平均累積補(bǔ)給水量分別為206.23和150.73 mm,砂層深埋(S2)處理分別為142.60和108.30 mm,兩個(gè)夾砂層處理的平均累積深層滲漏水量分別為331.19、164.18與214.73、117.96 mm。與S1處理相比,不含夾砂層(B)處理在40和120 cm深度處土壤水分向補(bǔ)給量分別增加36.38%、57.01%,較S2分別增加97.23%、118.53%,深層滲漏量較S1分別增加0.17%、60.64%,較S2分別增加80.45%、123.58%。
在不同生育期,含夾砂層處理與不含夾砂層處理在主要根系區(qū)和120 cm深度處的土壤水分深層滲漏量相差較大,滲漏量從大到小依次為B、S1、S2。40與120 cm深度處的土壤水分通過毛管作用向上補(bǔ)給主要在玉米拔節(jié)期開始增大,不含夾砂層處理向上層補(bǔ)給水量較大。主要根系區(qū)與120 cm土層深度處土壤水分深層滲漏與毛管上升補(bǔ)給各處理各生育期均隨灌水量增加而增大,S1處理下120 cm深度處W1、W2、W3滲漏量分別為灌溉水量的34.91%、28.56%、43.97%,S2處理分別為23.10%、16.66%、36.62%,B處理分別為13.32%、66.04%、85.77%。隨灌水量增大含夾砂層處理向主要根系層補(bǔ)給水量較為穩(wěn)定,無增加趨勢,而不含夾砂層處理隨灌水量增加主要根系層補(bǔ)給水量增加明顯,BW2與BW3較BW1分別增加27.5%、109.52%。由于砂層與土層對(duì)土壤水分的持蓄能力不同,含夾砂層處理土層在玉米苗期的土壤貯水量較不含夾砂層處理小,各處理生育期初期土壤貯水量如圖9所示。不含夾砂層處理在相同灌水下更易造成的土壤水分深層滲漏損失,砂層埋深較大時(shí),砂層以上土層較厚,土壤貯水量較大,表層土壤含水率較高,土壤負(fù)壓較低,使深層土壤水分通過毛管作用向上補(bǔ)給較少,同時(shí)在灌水后向砂層以下深層滲漏較少。
利用HYDRUS-1D模擬玉米生育期各處理根系吸水量,結(jié)果如圖10所示。兩個(gè)砂層埋深(S1、S2)處理與不含夾砂層(B)處理,玉米不同生育期的根系吸水量從大到小排序均為:灌漿期、灌漿期-成熟期、抽雄期、拔節(jié)期、苗期。隨著砂層埋深增加,作物根系受土壤水分脅迫減弱,S2處理玉米根系吸水量較S1處理在玉米抽雄期、灌漿期、灌漿-成熟期分別增大5.95%、3.12%、2.87%,B處理較S1處理根系吸水量分別增加5.70%、5.59%、10.28%,表明不含夾砂層處理較含夾砂層處理在3個(gè)需水量較大的生育期根系吸水脅迫更小,全生育期砂層淺埋與深埋處理根系吸水量分別為潛在蒸散量的55.51%、61.31%,B處理為66.69%。含夾砂層處理在不同灌水量下的根系吸水量無明顯變化,表明在夾砂層埋深不同時(shí),土壤質(zhì)地是影響玉米根系吸水量的主要因素。
利用HYDRUS-1D模擬的作物蒸騰量與根系吸水量計(jì)算暫時(shí)性水分虧缺量,利用實(shí)測產(chǎn)量數(shù)據(jù)與降雨量和灌溉量數(shù)據(jù)計(jì)算水分生產(chǎn)力,結(jié)果見圖11。由圖7可知,灌漿期玉米葉面積指數(shù)顯著大于其他生育期(<0.05),不同處理灌漿期葉面積指數(shù)平均為5.51,表明該時(shí)期玉米葉片對(duì)地表遮蓋率較高,需水主要以蒸騰為主。由圖 11可知,各處理的暫時(shí)性水分虧缺都在玉米抽雄期或灌漿期開始出現(xiàn),由于玉米灌漿期是玉米籽粒形成期,是其生長的關(guān)鍵時(shí)期[27],灌漿期間作物耗水量較多[28],無效的蒸騰水量過多會(huì)使玉米葉片暫時(shí)萎蔫與減產(chǎn)[29]。砂層淺埋時(shí),灌漿期3個(gè)灌水水平W1、W2、W3處理下的暫時(shí)水分虧缺量分別為121.88、27.95、76.05 mm,砂層深埋時(shí)分別為149.38、100.20、19.52 mm,不含夾砂層處理分別為72.20、58.23、6.04 mm,砂層深埋處理暫時(shí)性虧缺水量較砂層淺埋時(shí)更大,而在整個(gè)生育期內(nèi)不含夾砂層處理的暫時(shí)性水分虧缺量較小,對(duì)玉米生長造成影響較小[30]。隨灌水量增大水分生產(chǎn)力減小,S1處理灌水量W2與W3較W1分別減小23.75%、38.56%,S2處理為20.17%、44.62%,B處理為9.06%、32.05%,在相同灌水處理下,砂層深埋時(shí),土壤水分生產(chǎn)力與不含夾砂層時(shí)相近。
夾砂層對(duì)土壤水分蒸發(fā)的影響主要體現(xiàn)為砂層對(duì)土壤水分垂向遷移的阻礙作用[8],同時(shí)在不同處理下玉米葉面積指數(shù)差異明顯,地表覆蓋率差異顯著,影響葉面蒸騰與棵間土壤蒸發(fā)之間的分配。隨著砂層埋深增大土壤蒸發(fā)量減少,田間蒸散量與玉米蒸騰量均增大,由于S2葉面積指數(shù)較S1處理大,使得在玉米生育期內(nèi)表層土壤水分蒸發(fā)較小,各處理除玉米抽雄期的蒸發(fā)量最?。ɡ塾?jì)為12.26 mm)外,蒸發(fā)量在其他各生育期與各處理之間無明顯變化,玉米葉片p在各生育期之間隨時(shí)間變化明顯,同時(shí)隨著砂層埋深增加,玉米p增大,S2的玉米葉片p較S1處理大8.41%。
玉米葉片通過蒸騰作用消耗根系吸收的水分,玉米根系吸水在不同砂層埋深表現(xiàn)出的根系吸水量差異明顯,相同土壤質(zhì)地下不同灌水處理之間的根系吸水量并不明顯,與吳元芝等[31]的研究結(jié)果一致,相較于其他因素,土壤質(zhì)地對(duì)根系吸水的影響最大。主要根系層的土壤水分通量與研究區(qū)域底部土壤水分通量分別反映砂層對(duì)砂層上下土層的土壤水分運(yùn)移的影響。玉米生育期內(nèi)隨著砂層厚度減小,土壤水分向根系層補(bǔ)給增大,不含夾砂層土壤處理對(duì)根系吸水脅迫最小。史文娟等[8,32]的研究表明,砂層對(duì)其以下土層毛管水運(yùn)動(dòng)沒有影響,當(dāng)毛管水上升到土砂界面時(shí)其上升速度開始減小,且砂層層位越高,土壤水分在砂層以上上升速度越小。反之隨著砂層埋深減小砂層以上土層在灌水后,上層土壤水分向下層滲漏速率增加,同時(shí)由于砂層的持水量較土層持水量更小,故在灌水后淺埋砂層的砂層以上土層土壤水分向下滲漏速度與滲漏量均大于砂層深埋的處理。通過比較相同夾砂層埋深與不同灌水量處理下的根系層土壤水分滲漏與補(bǔ)給得出:隨著灌水量增加,土壤水分向根系層補(bǔ)給與滲漏同時(shí)增大,但是當(dāng)灌水量超過土層所能儲(chǔ)蓄的最大水量水分會(huì)通過砂層向下滲漏損失造成水分的浪費(fèi)[33],其次由于砂層含水量較小,造成由于負(fù)壓引起的不導(dǎo)水孔隙形成,夾砂層會(huì)阻礙土壤水分滲漏與土壤毛管水分上升的水分補(bǔ)給。綜合考慮土壤水分滲漏損失與土壤水分生產(chǎn)力,將灌水量控制在W2(315.85 mm)水平,既可以增大土壤水分向根系層的補(bǔ)給量的同時(shí)減小水分的滲漏損失。
由于夾砂層淺埋處理玉米葉面積較小使玉米蒸騰量較小[34],致使砂層深埋處理玉米水分虧缺量較砂層淺埋時(shí)大。不含夾砂層土壤暫時(shí)性水分虧缺量遠(yuǎn)小于含夾砂層處理。
綜上,含有夾砂層耕地土壤水分運(yùn)移規(guī)律與普通耕地差異較大。同時(shí),由于確定各土層土壤質(zhì)地時(shí),土鉆鉆孔取樣深度存在一定的試驗(yàn)誤差,導(dǎo)致實(shí)際農(nóng)田砂層分布與模型中輸入的砂層分布的幾何信息之間存在一定的差異。本研究仍需要進(jìn)一步改進(jìn),比如用尋找更加簡單精確的方式確定耕地各土層的土壤質(zhì)地與空間分布的方法,進(jìn)一步改進(jìn)模型,考慮夾砂層結(jié)構(gòu)對(duì)玉米生長的影響機(jī)制等。在農(nóng)業(yè)水資源緊張,要求高效灌溉的背景下,灌水應(yīng)結(jié)合灌區(qū)特殊土壤條件,對(duì)灌區(qū)的灌溉制度與灌溉策略進(jìn)一步優(yōu)化。
本文利用HYDRUS-1D模型模擬了河套灌區(qū)典型土壤下土壤水分運(yùn)動(dòng),模擬研究了不同砂層埋深下玉米農(nóng)田蒸散量變化規(guī)律、土壤水分補(bǔ)給與滲漏過程、根系吸水與水分虧缺變化規(guī)律。得出如下結(jié)論:
1)較不含夾砂層處理,含夾砂層的玉米田間土壤水分蒸發(fā)損失大,葉面蒸騰耗水分配較少。隨著夾砂層埋深增加,玉米棵間土壤蒸發(fā)減小,分配至葉面蒸騰耗水增加,在此研究中砂層深埋較砂層淺埋處理棵間土壤蒸發(fā)損失水量減小13.60%。
2)隨夾砂層埋深減小,主要根系層貯水量減小,土壤水分深層滲漏量減小,砂層以上土層向上補(bǔ)給水量減小。不含夾砂層處理較淺埋砂層與深埋砂層處理田間土壤貯水量更大,使玉米生育期內(nèi)120 cm深度處滲漏量更多,但由于不受砂層阻水作用影響,不含夾砂層處理玉米田間毛管向上補(bǔ)給水量較淺埋砂層與深埋砂層處理分別大57.01%、118.53%。隨灌水量增加不含砂層處理田間土壤水分深層滲漏與補(bǔ)給均增加,灌水量為315.85 mm時(shí)含夾砂層處理的土壤水分深層滲漏最小。
3)玉米生育期內(nèi)根系吸水量隨砂層埋深的增加而增大,不含夾砂層處理根系吸水受到水分脅迫最小,根系吸水量最大。砂層淺埋與砂層深埋處理根系吸水量分別為潛在蒸散量的55.51%、61.31%,不含夾砂層處理為66.69%。
4)砂層深埋處理在玉米生育期暫時(shí)性虧缺水量最大,水分生產(chǎn)力從大到小排序?yàn)椋翰缓皩犹幚?、砂層深埋、砂層淺埋。當(dāng)灌水量為315.85 mm時(shí),土壤水分生產(chǎn)力減少最小。
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Water use analysis of cultivated land with typical sand layers in Hetao Irrigation District of Inner Mongolia using HYDRUS-1D model
Feng Zhuangzhuang, Shi Haibin※, Miao Qingfeng, Sun Wei, Liu Meihan, Dai Liping
(1.,,010018,; 2.010018,)
Extensive sand layers are widely distributed over the impact plain of the Yellow River, particularly for Hetao Irrigation Areas in Inner Mongolia of western China. The migration of water and salt under the soil sand layer has posed a great influence on soil water utilization, soil salinization control, and crop growth. In this study, a numerical model of soil water movement was proposed to investigate the field evapotranspiration, crop water consumption, water supply, and deep soil water leakage in the sand layer using the data of field monitoring and laboratory experiments during the growth period of spring maize. Taking the cultivated land of the typical sand layer in the Hetao Irrigation Area as the research object and planting crop as spring corn, two gradients of buried depth were selected: S1 (40-95 cm) and S2 (60-110 cm) of the sand layer in the soils. Three irrigation levels were also set to carry out the field experiment, and then to compare with BWI without sand layer, including W1 (252.5 mm), W2 (315.85 mm), and W3 (378.75 mm). A HYDRUS-1D model was selected to simulate the field evapotranspiration during the growth period of spring maize, deep seepage of soil water, groundwater recharge, and root water absorption. In addition, the temporary water deficit and water productivity were calculated during the whole growth period. Water use in the cultivated land with sand layer was then compared with that without sand layer. The results showed that the soil evaporation loss between grains decreased, whereas, the leaf transpiration water increased, with the increase of buried depth of the sand layer. Specifically, the soil layer above the sand layer was thicker, the soil water storage was larger, the surface soil moisture content was higher, and the soil negative pressure was lower when the buried depth of the sand layer was larger. As such, the deep soil water was less replenished upward through the capillary action. At the same time, there was less leakage to the deep layer below the sand layer after irrigation. Furthermore, the upstream water supply of maize in the field without sand layer increased by 57.01% and 118.53%, respectively, compared with the treatment of shallow (40-95 cm), and deep sand layer (60-110 cm). More importantly, the deep-water leakage of soil under the treatment of sand layer was the least, when the irrigation amount was 315.85mm. Correspondingly, the water absorption of maize roots decreased with the increase in the buried depth of the sand layer, where the largest was found without sand layer during the growth period. Specifically, the shallow (40-95 cm) and deep sand layer (60-110 cm) treatment were 55.51% and 61.31% of evapotranspiration, respectively, whereas, the treatment without sand layer was 66.69%. The irrigation system can be determined for spring maize in the sand layer, according to the sand layer distribution and local conditions. Particularly, the recommended irrigation quota of spring corn can be 315.85 mm during the growth period, when the sand layer was similar to the S1WI and S2WI treatment. The recommendation can be attributed to avoiding the leakage loss of irrigation water in the deep soil water of the farmland with the sand layer. The findings can also provide important theoretical guidance for the formulation of a farmland irrigation system with the sand layer in the Hetao Irrigation District.
irrigation; soil water content; sand-layered soil; soil transpiration; groundwater recharge; deep seepage; HYDRUS-1D model
馮壯壯,史海濱,苗慶豐,等. 基于HYDRUS-1D模型的河套灌區(qū)典型夾砂層耕地水分利用分析[J]. 農(nóng)業(yè)工程學(xué)報(bào),2021,37(18):90-99.doi:10.11975/j.issn.1002-6819.2021.18.011 http://www.tcsae.org
Feng Zhuangzhuang, Shi Haibin, Miao Qingfeng, et al. Water use analysis of cultivated land with typical sand layers in Hetao Irrigation District of Inner Mongolia using HYDRUS-1D model[J]. Transactions of the Chinese Society of Agricultural Engineering (Transactions of the CSAE), 2021, 37(18): 90-99. (in Chinese with English abstract) doi:10.11975/j.issn.1002-6819.2021.18.011 http://www.tcsae.org
2021-05-15
2021-08-18
國家自然科學(xué)基金項(xiàng)目(51769024);國家基金重點(diǎn)項(xiàng)目(51539005)
馮壯壯,研究方向?yàn)楣?jié)水灌溉理論與新技術(shù)。Email:1445820101@qq.com
史海濱,博士,教授,研究方向?yàn)楣?jié)水灌溉理論與新技術(shù)。Email:shi_haibin@sohu.com
10.11975/j.issn.1002-6819.2021.18.011
S274
A
1002-6819(2021)-18-0090-10