欒國(guó)強(qiáng)，董春梅,2，林承焰,2，任麗華,2，焦紅巖，趙海燕，彭先國(guó)[.中國(guó)石油大學(xué)(華東) 地球科學(xué)與技術(shù)學(xué)院，山東 青島 266580； 2.山東省油藏重點(diǎn)實(shí)驗(yàn)室，山東 青島 266580；.中國(guó)石化 勝利油田有限公司 現(xiàn)河采油廠，山東 東營(yíng) 257068]

1 異重流研究歷史

廣義的異重流指兩種密度相差不大、可以相混的流體，在條件適宜時(shí)因密度差異而產(chǎn)生的相對(duì)運(yùn)動(dòng)。在運(yùn)動(dòng)過(guò)程中不發(fā)生全局性紊動(dòng)、摻混。異重流分為雙層體系和多層體系，自然界中異重流現(xiàn)象非常廣泛，既包括水體中的分層潛流，也包括大氣中的冷暖空氣所形成的鋒面。但在水利工程和地質(zhì)學(xué)領(lǐng)域，異重流是指河流攜帶大量沉積物直接潛入蓄水盆地底部并繼續(xù)流動(dòng)的高密度流體[1-3]。

1885年Forel首次報(bào)道了羅恩河注入日內(nèi)瓦湖時(shí)發(fā)生的異重流現(xiàn)象[4]，20世紀(jì)30年代以后，異重流研究才真正受到重視。1935年美國(guó)科羅拉多河胡佛壩落成蓄水，當(dāng)年3月份，上游發(fā)生洪水，河流攜大量泥沙在胡佛大壩前沉入水底，不久后渾濁的泥水從大壩泄水孔流出，在此過(guò)程中水庫(kù)表面始終澄清[5]。這一現(xiàn)象讓人們意識(shí)到異重流可以攜帶大量泥沙沿水庫(kù)底部長(zhǎng)距離搬運(yùn)而不與蓄水體相混，這對(duì)于降低水庫(kù)淤積，延長(zhǎng)水庫(kù)壽命具有重要意義。1953年Bates首次提出異重流的概念，但在地質(zhì)領(lǐng)域，對(duì)于海洋環(huán)境中是否存在異重流及其對(duì)海相深水沉積的影響卻仍然存在巨大爭(zhēng)議。直到20世紀(jì)90年代，相關(guān)研究表明河流入海形成異重流的現(xiàn)象具有普遍性[2,6]，異重流作為一種深水沉積物輸送機(jī)制逐漸受到地質(zhì)學(xué)家的重視[7-42](表1；圖1)。

2 異重流形成條件與影響因素

2.1 形成條件

河流與蓄水體的密度差異是異重流發(fā)生的直接原因[2,6,24,43-48]。河流所攜沉積物量、水體鹽度及溫度等都是影響河水密度的重要因素[49]。河流入海形成異重流的沉積物臨界濃度為36～44 kg/m3，臨界濃度與海水溫度和含鹽度密切相關(guān)，受氣候背景和所處緯度控制[2](表2)。洪峰到達(dá)前河流對(duì)蓄水體的稀釋作用[50]會(huì)降低河口處蓄水體密度，有利于異重流的發(fā)生。嚴(yán)格來(lái)講，異重流形成的臨界濃度是蓄水體密度(河口周?chē)?、流量、水深和坡降的函數(shù)，河口處坡度大、水體深，形成異重流的沉積物臨界濃度也會(huì)相應(yīng)降低。在陸相淡水湖盆中，異重流形成的沉積物臨界濃度非常低(遠(yuǎn)低于1 kg/m3)[2,51]。如果河水與湖水溫度和鹽度相差不大，河水所攜帶沉積物濃度只要略大于千分之一，入湖后便可以形成異重流[52]。通常來(lái)說(shuō)，洪泛期的中小型山區(qū)河流更易形成異重流，而大型河流由于流速低，流量大，入海過(guò)程中沉積物易發(fā)生稀釋和卸載，難以形成異重流[6]。Mulder等調(diào)研了全球147條河流的異重流發(fā)育情況，發(fā)現(xiàn)71%的河流會(huì)發(fā)育不同頻次的異重流[2]，而實(shí)際上異重流的發(fā)生可能更加普遍。

不穩(wěn)定的異輕流可以向異重流轉(zhuǎn)化，這是一種特殊而普遍的異重流形成機(jī)制[25,32,53]。溫暖的富含細(xì)粒沉積物的河水在河口形成異輕流，在沉積物自身擴(kuò)散和水體擾動(dòng)(波浪、潮汐等作用)影響下，異輕流與蓄水體界面之間的平衡被破壞，發(fā)生指對(duì)流現(xiàn)象(finger convection)，富沉積物流體通過(guò)指對(duì)流到達(dá)盆地底部，形成異重流[53](圖2)。通過(guò)指對(duì)流機(jī)制產(chǎn)生的異重流，其主要沉積物為富含陸源有機(jī)質(zhì)的粘土[25]。如果異輕流長(zhǎng)時(shí)間保持穩(wěn)定，所含細(xì)粒沉積物會(huì)發(fā)生絮凝作用，以海洋雪的方式沉降[54]。

2.2 主要影響因素

異重流的形成受構(gòu)造和氣候影響，與源匯系統(tǒng)密切相關(guān)。

2.2.1 源區(qū)特征

一定的沉積物濃度是異重流形成的重要條件[48,55]，如果源區(qū)能夠提供大量的碎屑物質(zhì)，則有利于異重流的形成。源區(qū)構(gòu)造演化與地形起伏是碎屑沉積物形成的基礎(chǔ)，母巖固結(jié)程度低，構(gòu)造高差大，易發(fā)生侵蝕搬運(yùn)作用。氣候是沉積物形成的重要條件，一般認(rèn)為半干旱氣候下，物源區(qū)植被稀少，容易發(fā)生水土流失[56]，同時(shí)伴隨周期性洪水的發(fā)生，有利于河流攜帶大量懸浮物質(zhì)形成異重流[48,57-58]。

2.2.2 河流流域

河流是源匯系統(tǒng)內(nèi)沉積物輸送的重要通道[59]，河流流域特征決定了河流類(lèi)型、流量及沉積物輸送能力[6,60]。河流從物源區(qū)攜帶的沉積物只有少部分能直接到達(dá)沉積盆地，其余大部分會(huì)在搬運(yùn)路途中發(fā)生暫時(shí)性沉積，形成心灘、邊灘、決口扇、山麓沖積扇及沖積平原等[61]，大量暫時(shí)性沉積的發(fā)生會(huì)緩沖河流向盆地搬運(yùn)沉積物的效率。一般來(lái)說(shuō)，流域面積越大，地形高差越低，河流輸送能力越差[6,62-65]。流域氣候條件也會(huì)對(duì)河流輸送能力產(chǎn)生重要影響，蒸發(fā)量大，導(dǎo)致河流流量降低，沉積物在河流區(qū)域大量攜載，不利于異重流發(fā)生。因此，相對(duì)于大型河流，中小型的山間河流因?yàn)榱饔蛎娣e小，高程大，蒸發(fā)量低，易于形成異重流[6]。

2.2.3 匯水盆地

蓄水體鹽度、水深、溫度以及河口坡降等都是影響河流潛入的重要因素，盆地水體鹽度低、溫暖、有一定水深和較大的河口坡降，會(huì)降低異重流形成的沉積物臨界濃度。異重流發(fā)生還與海/湖平面高低有密切關(guān)系[26,48,66-73]，在狹窄大陸架條件下，低水位體系域時(shí)，河流可直接進(jìn)入大陸坡峽谷，有利于異重流的形成；而在寬闊大陸架地帶，低水位體系域時(shí)，河流流域面積增大，中小型河流發(fā)生合并，形成大河，更利于三角洲和滑塌型重力流的發(fā)生。

表1 異重流沉積研究實(shí)例Table 1 Case study of hyperpycnal flow deposition

圖1 異重流沉積研究實(shí)例全球分布示意圖Fig.1 Global distribution of case study of hyperpycnal flow deposition

表2 不同氣候環(huán)境下海水溫度、鹽度、密度及對(duì)應(yīng)的河流沉積物臨界濃度(引自文獻(xiàn)[2])Table 2 Temperature,salinity and density of seawater in different climates,and the correspondingcritical concentration of river sediments(cited from reference [2])

3 異重流演化過(guò)程及沉積特征

3.1 演化過(guò)程

在洪水到達(dá)之前，由于河水中所攜帶沉積物濃度低，河水密度低于蓄水體密度，在河口處粗碎屑物質(zhì)卸載，形成三角洲河口沙壩，河水緩慢向前漂浮在蓄水體表面，形成異輕流(圖3a)。隨著洪水發(fā)育，河流攜帶沉積物濃度越來(lái)越大，當(dāng)河水濃度與蓄水體濃度相等時(shí)，河水與海水整體混合，形成等密度流(圖3b)。在洪水作用下，河流流速加快，所攜帶沉積物濃度增加，河水密度大于蓄水體密度，達(dá)到潛入臨界條件，河流直接潛入水底，形成向盆地深處運(yùn)移的異重流(圖3c)。異重流的發(fā)生會(huì)帶動(dòng)周?chē)w的運(yùn)動(dòng)，形成局部水循環(huán)，倒吸先前漂浮在水面的異輕流，大量水體表面漂浮物在潛入點(diǎn)處聚集，形成分明的清渾交界面(圖4a)。

圖2 尼羅河河口異輕流-異重流轉(zhuǎn)化作用(據(jù)文獻(xiàn)[25]修改)Fig.2 Conversion from hypopycnal flow to hyperpycnal flow at the estuary of Nile River(modified from reference [25])

在海洋和鹽湖環(huán)境中，如果異重流頭部速度過(guò)低，其所攜帶沉積物的濃度小，局部密度低于周?chē)w密度，會(huì)發(fā)生浮力反轉(zhuǎn)，形成上浮相(圖3，圖4)，上浮相開(kāi)始產(chǎn)生的位置為上浮點(diǎn)，上浮點(diǎn)位置隨異重流頭部運(yùn)動(dòng)發(fā)生遷移，在異重流增強(qiáng)期，上浮點(diǎn)隨異重流向盆運(yùn)動(dòng)，在異重流衰退期，上浮點(diǎn)隨異重流向岸運(yùn)動(dòng)(圖3c—f)。上浮點(diǎn)的運(yùn)移方式有連續(xù)運(yùn)移和幕式運(yùn)移，這取決于異重流能量演化特征。上浮相與異重流所攜帶的沉積物類(lèi)型和流速有密切關(guān)系，以粘土為主的異重流不易產(chǎn)生上浮相[74]。異重流衰退末期完全上浮，回歸等密度流和異輕流(圖3g，h)。

3.2 主要巖相類(lèi)型

異重流存在3種沉積物搬運(yùn)方式——底床載荷、懸浮載荷和上浮載荷(圖5)。其中底床載荷沉積物主要以滾動(dòng)和跳躍方式搬運(yùn)；懸浮載荷是異重流主要沉積物運(yùn)載方式，沉積物以懸浮狀態(tài)發(fā)生搬運(yùn)；上浮載荷是指異重流末端沉積物大量卸載，異重流密度低于環(huán)境水體密度后，沉積物發(fā)生上浮擴(kuò)散的一種搬運(yùn)方式，主要發(fā)生在海相和鹽湖環(huán)境中。

異重流沉積的巖相類(lèi)型與沉積物負(fù)載方式密切相關(guān)[75-77]，底床載荷主要沉積細(xì)礫巖與礫質(zhì)砂巖，常見(jiàn)的沉積構(gòu)造有塊狀層理、疊瓦狀構(gòu)造、低角度交錯(cuò)層理、平行層理等。懸浮載荷主要沉積細(xì)砂巖、粉砂巖，典型的沉積構(gòu)造有平行層理、爬升沙紋層理、波狀層理等。沉積物重新聚集和上浮部分主要沉積水平層理泥巖和粉砂質(zhì)泥巖，層面富含有機(jī)質(zhì)和異地搬運(yùn)的植物碎屑[78](圖5)。異重流由近源到遠(yuǎn)源過(guò)程中，能量虧損，流速降低，底床載荷、懸浮載荷和上浮載荷依次卸載形成特有的沉積序列。

3.3 沉積序列

單期異重巖沉積過(guò)程與異重流能量演化過(guò)程密切相關(guān)，因此異重巖垂向沉積序列記錄了異重流能量增強(qiáng)和減弱兩個(gè)演化階段[24](圖3，圖6，圖7)。在洪水發(fā)育初期，異重流能量不斷增強(qiáng)，沉積物具有反序特征，并依次發(fā)育爬升波紋層理、平行層理和低角度交錯(cuò)層理等沉積構(gòu)造；洪峰過(guò)后，隨著洪水能量衰減，異重流所攜帶沉積物由粗到細(xì)依次卸載，沉積物具有正序特征，沉積構(gòu)造與異重流能量增強(qiáng)階段相反。這種反映洪水能量增強(qiáng)的反序沉積單元(Ha)和反映洪水能量減弱的正序沉積單元(Hb)所組成的二元結(jié)構(gòu)是異重巖典型沉積序列(圖6)[9,24,33,74,79-80]。異重流除了經(jīng)歷增強(qiáng)和減弱兩個(gè)大的變化階段外，同一位置異重流能量會(huì)有多次波動(dòng)(圖6)，這一特點(diǎn)體現(xiàn)為異重流流動(dòng)過(guò)程的脈動(dòng)性。

洪峰活動(dòng)期間，如果異重流能量未達(dá)到對(duì)下伏沉積物造成侵蝕的臨界條件，Ha與Hb之間連續(xù)接觸，沉積物最大粒度代表的接觸界面響應(yīng)于洪峰(圖6Ⅲ，圖7Ⅲ)；如果洪峰期間異重流能量超過(guò)對(duì)下伏沉積物造成侵蝕的臨界條件，異重流能量增強(qiáng)階段形成的沉積物會(huì)被部分侵蝕，洪峰過(guò)后隨異重流能量減弱，沉積物繼續(xù)在侵蝕面之上沉積，Ha與Hb侵蝕接觸(圖6Ⅱ，圖7Ⅱ)；當(dāng)洪峰能量足夠大，持續(xù)時(shí)間足夠長(zhǎng)，異重流能量增強(qiáng)階段形成的反序單元(Ha)在洪峰期會(huì)被完全侵蝕，洪峰過(guò)后隨異重流能量降低，沉積物卸載，僅保存正序單元(Hb)(圖6Ⅰ，圖7Ⅰ)。實(shí)際上由于河流注入量和所攜帶沉積物濃度的變化，異重流存在多個(gè)能量波動(dòng)過(guò)程[41]，導(dǎo)致單期異重巖沉積序列更加復(fù)雜。異重流不僅有時(shí)間上的波動(dòng)性，還有空間上的遲滯性。離河口越遠(yuǎn)，異重流速度越低，一期洪峰總是先到達(dá)近端，一段時(shí)間之后才能傳播到遠(yuǎn)端(圖6)，導(dǎo)致同一能量波動(dòng)在不同位置異重巖中的時(shí)間響應(yīng)不同，同一期異重流在不同位置形成的沉積序列不同(圖7)。

圖3 異重流演化過(guò)程[74] Fig.3 Evolution of hyperpycnal flow[74] a.洪水初期，異輕流發(fā)育；b.隨洪水能量增強(qiáng)，河流攜帶沉積物濃度達(dá)到臨界濃度，等密度流形成；c.隨洪水能量增強(qiáng)，異重流形成并加速向深水流動(dòng)；d.洪峰到達(dá)，異重流能量達(dá)到最強(qiáng)；e.洪峰之后，異重流能量開(kāi)始衰減；f.異重流能量進(jìn)一步衰減；g.異重流衰減為等密度流；h.洪水過(guò)后，等密度流恢復(fù)為異輕流

圖4 紅海阿卡巴灣異重流[28]Fig.4 Hyperpycnal flows in the Gulf of Aqaba,Red Sea[28]a.異重潛入點(diǎn)處清渾交界；b,c.異重流表面上浮相

圖5 異重巖主要巖相類(lèi)型[74]Fig.5 Major lithofacies of hyperpycnites[74]

異重流近端洪峰期能量強(qiáng)，對(duì)下伏沉積物侵蝕強(qiáng)烈，以正序水道充填沉積為主；中部洪峰期異重流能量中等，形成侵蝕接觸的Ha-Hb二元結(jié)構(gòu)，侵蝕面附近富含泥礫。遠(yuǎn)端洪峰期異重流能量低，形成連續(xù)接觸的Ha-Hb二元結(jié)構(gòu)(圖6，圖7)。

圖6 異重流沉積演化過(guò)程(據(jù)文獻(xiàn)[9]修改)Fig.6 Depositional evolution of hyperpycnal flows (modified from reference [9])

圖7 異重流沉積序列(圖中Ⅰ,Ⅱ,Ⅲ位置與圖6中Ⅰ,Ⅱ,Ⅲ位置相對(duì)應(yīng))Fig.7 Sedimentary sequence of hyperpycnal flows (location Ⅰ，Ⅱand Ⅲ are also the location Ⅰ，Ⅱand Ⅲ in Fig.6)

3.4 沉積模式

河流攜帶沉積物直接入水所形成的異重流沉積與盆內(nèi)滑塌型濁流存在差異。本文在總結(jié)阿根廷內(nèi)烏肯盆地、美國(guó)阿巴拉契亞盆地、中國(guó)的松遼盆地和鄂爾多斯盆地等古代異重流沉積的基礎(chǔ)上，結(jié)合地中海現(xiàn)代深水水道發(fā)育特征，建立了由溝道充填沉積-天然堤-溝道側(cè)緣沉積-前緣朵葉體組成的異重流沉積的理想模式(圖8)。異重流沉積近端，由于能量較強(qiáng)，侵蝕作用顯著，溝道陡深，由近端向遠(yuǎn)端逐漸變寬緩，溝道底部充填底負(fù)載相的細(xì)礫巖和礫質(zhì)砂巖，向上依次為懸浮相細(xì)砂巖、粉砂巖和上浮相泥巖，具有顯著的正序特征。兩側(cè)天然堤主要由懸浮相的細(xì)砂巖、粉砂巖和上浮相泥質(zhì)粉砂巖、泥巖組成，由溝道向兩側(cè)粒度減小，泥質(zhì)含量增加，逐漸過(guò)渡到溝道側(cè)緣沉積。溝道側(cè)緣沉積主要由上浮相的泥質(zhì)粉砂巖、粉砂質(zhì)泥巖和泥巖組成，常見(jiàn)大量植物碎屑和紅色層理。在異重流沉積前緣末端，由于沒(méi)有溝道約束，沉積物大量溢出，形成以懸浮相和上浮相為主的前緣朵葉體，該部分沉積物與天然堤和側(cè)緣沉積相似，具有典型的Ha-Hb二元結(jié)構(gòu)。

4 討論

4.1 異重流與經(jīng)典濁流的區(qū)別

沉積物重力流包括盆內(nèi)滑塌型重力流和盆外洪水型異重流[81-82]，兩類(lèi)重力流在成因機(jī)制、流體動(dòng)力學(xué)過(guò)程及沉積特征等方面都存在差異性，進(jìn)一步造成油氣儲(chǔ)層分布的不同[21,82]。同時(shí)，由于傳統(tǒng)的涌浪型濁流與異重流存在相似性，致使在以往研究中有大量異重流沉積被解釋為經(jīng)典濁流沉積[9]。因此認(rèn)識(shí)傳統(tǒng)濁流沉積與異重流沉積的區(qū)別與聯(lián)系，對(duì)于建立和完善深水重力流沉積模式具有重要意義。

圖8 異重流沉積模式Fig.8 Depositional model of hyperpycnal flows

根據(jù)Ha-Hb二元結(jié)構(gòu)、內(nèi)部侵蝕突變界面、富含陸源植物碎屑等特征可以從巖心和露頭對(duì)異重流和經(jīng)典濁流沉積進(jìn)行初步識(shí)別，但更多的識(shí)別標(biāo)志仍需要進(jìn)一步發(fā)掘，兩種不同沉積的地球物理差異性仍然有待研究(表3)。

在實(shí)際研究中，三角洲地帶往往存在三角洲-異重流-盆內(nèi)重力流綜合沉積作用(圖9)[83]。洪水期間異重流的發(fā)生可以作為觸發(fā)機(jī)制，造成斜坡失穩(wěn)，產(chǎn)生盆內(nèi)重力流，導(dǎo)致多種重力流事件同時(shí)發(fā)生[20,84]；進(jìn)積型三角洲帶來(lái)的沉積物大量堆積，也可以為盆內(nèi)重力流提供物質(zhì)基礎(chǔ)，導(dǎo)致盆外和盆內(nèi)重力流交替發(fā)生。盆內(nèi)和盆外重力流的混合發(fā)育以及復(fù)雜的流體轉(zhuǎn)化過(guò)程，增加了重力流研究的挑戰(zhàn)性。

4.2 異重流與細(xì)粒沉積

異重流對(duì)深水細(xì)粒沉積有重要影響。細(xì)粒沉積物形成于弱水動(dòng)力條件一直是沉積學(xué)界的共識(shí)，然而近年來(lái)沉積學(xué)家們通過(guò)大量的實(shí)際觀察和實(shí)驗(yàn)研究逐漸認(rèn)識(shí)到,在較強(qiáng)水動(dòng)力條件下也可以沉積細(xì)粒物質(zhì)[85-89]。異重流是細(xì)粒沉積物重要的運(yùn)載方式之一[48,74,81,90]，異重流中的懸浮相和上浮相都以細(xì)粒沉積物為主，泥質(zhì)異重流和通過(guò)指對(duì)流方式形成的異重流所攜沉積物以粘土為主，異重流可以攜帶大量陸源細(xì)粒沉積物直接進(jìn)入深水形成細(xì)粒沉積，對(duì)正常深水環(huán)境產(chǎn)生重要影響。

洪水期間，泥質(zhì)異重流從三角洲前緣溢出，可在平緩的地形條件下將大量陸源細(xì)粒沉積物輸送上百千米，在近海大陸架形成大規(guī)模泥質(zhì)沉積。這種成因的細(xì)粒沉積巖在淺海陸架地區(qū)具有普遍性，被稱(chēng)為泥質(zhì)前三角洲異重巖[29]。泥質(zhì)前三角洲異重巖通常由粉砂巖和泥巖組成，單層厚度為厘米尺度，下部發(fā)育侵蝕面。單層內(nèi)部主要由3部分組成，下部為發(fā)育脈動(dòng)式牽引流特征的泥質(zhì)粉砂巖或粉砂質(zhì)泥巖，中間為無(wú)明顯宏觀特征的泥巖，最上部為發(fā)育大量生物變形構(gòu)造的泥巖[29](圖10)。單層的沉積過(guò)程大致可分為3個(gè)階段，首先是過(guò)路侵蝕階段，形成下部的侵蝕界面，之后在異重流能量虧損階段，開(kāi)始沉積形成下部的泥質(zhì)粉砂巖、粉砂質(zhì)泥巖(推移質(zhì))和中間的泥巖(懸浮質(zhì))，最后形成上部的暗色泥巖并發(fā)育生物擾動(dòng)(圖10)。

表3 異重流與經(jīng)典濁流沉積差異對(duì)比Table 3 Similarities and differences between typical turbidites and hyperpycnal flows

圖9 三角洲-異重流-滑塌重力流綜合沉積模式Fig.9 Composite depositional model of delta,hyperpycnal flow,and slumping gravity flow

由于異重流能量的波動(dòng)性，泥質(zhì)前三角洲異重巖在單層系和層系組級(jí)別發(fā)育正粒序和反粒序，但在幾十到上百米的準(zhǔn)層序級(jí)別具有向上變粗變厚的反序特征[32]。

異輕流、層間流、滑塌型重力流都是深水細(xì)粒沉積物的重要供給方式，但異重流特殊性在于將河水和陸源沉積物直接輸送到盆地底部，大量陸源物質(zhì)的加入，會(huì)改變深層水體含氧量、含鹽度等物理化學(xué)性質(zhì)，從而對(duì)原地有機(jī)質(zhì)的保存產(chǎn)生影響，同時(shí)形成大量陸源有機(jī)質(zhì)沉積[32,79,91]。

4.3 中國(guó)陸相湖盆異重流沉積研究

相比于海相環(huán)境，陸相湖盆由于水體鹽度低、物源近、以中小型河流為主等特點(diǎn)，更容易發(fā)生異重流。楊仁超等(2017)從構(gòu)造和氣候角度，對(duì)鄂爾多斯盆地異重流沉積特征開(kāi)展研究，并提出了異重巖測(cè)井識(shí)別標(biāo)志[21]。馮志強(qiáng)等(2010)發(fā)現(xiàn)松遼盆地嫩江組發(fā)育大規(guī)模湖底水道系統(tǒng)，起源于杏樹(shù)崗三角洲，在平緩的湖底延伸70 km，最后成扇體撒開(kāi)(圖11)，巖心中發(fā)育植物葉片、平行層理和交錯(cuò)層理[92]，綜合分析這些特征，可初步判斷為異重流沉積。我國(guó)陸相湖盆普遍發(fā)育的洪水型湖底扇，其形成機(jī)制及沉積特征都與底負(fù)載型異重流類(lèi)似。渤海灣盆地濟(jì)陽(yáng)坳陷東營(yíng)三角洲在沙三中亞段發(fā)生大規(guī)模進(jìn)積，同時(shí)形成了一系列滑塌濁積體，是巖性油氣藏勘探重點(diǎn)區(qū)塊[93-94]，但巖心觀察發(fā)現(xiàn)，該地區(qū)存在大規(guī)模異重流沉積過(guò)程(圖12)，有效區(qū)分滑塌濁積和異重流沉積，對(duì)于進(jìn)一步推動(dòng)該地區(qū)的勘探工作有重要意義。

圖10 紐約中部中泥盆世杰納西奧組細(xì)粒沉積巖異重流沉積模式及理想巖相特征[29] Fig.10 Depositional model and idealized lithofacies features of hyperpycnal flows with fine-grained sedimentary rocks in the Middle Denovian Genesee Formation,central New York[29]a. Northern Appalachian盆地泥盆世素描圖，發(fā)生異重流沉積;b.圖a中沿A—B剖面圖，異重流發(fā)育底負(fù)載、懸浮負(fù)載和上浮負(fù)載;c.理想泥質(zhì)異重流巖相序列素描圖

圖11 松遼盆地嫩江組陸相湖盆湖底水道體系(據(jù)文獻(xiàn)[92]修改)Fig.11 Bottom channel system of a continental lacustrine basin in the Neijiang Formation,Songliao Basin(modified from reference [92])

圖12 東營(yíng)凹陷沙三中亞段異重流沉積構(gòu)造Fig.12 Sedimentary structure of hyperpycnal flows in the middle Es3,Dongying saga.上攀層理，濱424井，埋深2 496.1 m；b.逆正粒序，局部炭質(zhì)碎屑成層富集，發(fā)育火焰狀構(gòu)造，說(shuō)明上部沉積時(shí)下部泥質(zhì)富含水，為同一期異重流能量波動(dòng)成因，牛116井，埋深3 102.1 m；c.層面富集植物碎片，河155井，埋深2 979.49 m；d.逆正粒序泥質(zhì)粉 砂巖，發(fā)育紅色層理，河155井，埋深3 002.4 m

5 結(jié)論

1) 異重流作為一種深水沉積物輸送機(jī)制，其發(fā)育具有普遍性。對(duì)異重流的成因機(jī)制、演化過(guò)程及沉積特征開(kāi)展研究有助于加深對(duì)深水重力流沉積的理解。有效區(qū)分異重流與盆內(nèi)滑塌型濁流，建立異重流沉積巖心-測(cè)井-地震識(shí)別標(biāo)志，完善異重流沉積模式，是異重流研究的當(dāng)務(wù)之急。

2) 異重流能夠沿相對(duì)平緩地形將陸源沉積物輸送上百公里，泥質(zhì)異重流對(duì)于盆地細(xì)粒沉積具有重要影響，異重流研究對(duì)于進(jìn)一步拓展隱蔽油氣藏勘探范圍，指導(dǎo)非常規(guī)油氣勘探具有重要意義。

3) 中國(guó)陸相湖盆異重流沉積研究處于起步階段，將異重流沉積體系與現(xiàn)有陸相湖盆沉積體系融合，建立陸相湖盆異重流沉積模式，必將進(jìn)一步推動(dòng)中國(guó)湖相油氣勘探進(jìn)程。

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