四川盆地早古生代構(gòu)造熱演化特征

何麗娟+黃方+劉瓊穎+李春榮+汪集旸

基金項(xiàng)目：中國石油化工股份有限公司海相前瞻性研究項(xiàng)目(YPH08101)

摘要：四川盆地位于揚(yáng)子板塊西緣,是中國重要的含油氣盆地之一，在震旦紀(jì)—早奧陶世處于裂陷特征的被動大陸邊緣階段。利用地球動力學(xué)理論在巖石圈尺度探討盆地構(gòu)造熱演化特征，恢復(fù)早古生代熱歷史，為盆地生烴狀態(tài)、生烴期次等研究提供重要熱參數(shù)。首先，利用回剝技術(shù)得到盆地構(gòu)造沉降史，并作為構(gòu)造熱演化模擬的目標(biāo)函數(shù)；然后，基于二維多期拉張模型，分別與晚震旦世、寒武紀(jì)和奧陶紀(jì)等3個(gè)時(shí)期構(gòu)造沉降量擬合得到3期拉張系數(shù)，揭示巖石圈底界和溫度場的演化以及基底熱流隨時(shí)間的演化特征。模擬結(jié)果顯示：在巖石圈拉張作用下，軟流圈上涌形成熱擾動，震旦紀(jì)時(shí)期基底熱流值略有升高，其中高值主要分布在盆地西北與西南，而川東北受到的影響最?。粺釘_動在寒武紀(jì)有所減弱，至奧陶紀(jì)時(shí)期基本消失，盆地?zé)崃髦党示徛陆第厔荩慌璧鼗谉崃髟谠绻派冀K在52~59 mW·m-2范圍內(nèi)。

關(guān)鍵詞：構(gòu)造熱演化；多期拉張模型；早古生代；基底熱流；巖石圈尺度；數(shù)值模擬；四川盆地

中圖分類號：P314.2文獻(xiàn)標(biāo)志碼：A

Tectonothermal Evolution of Sichuan Basin in Early Paleozoic

HE Lijuan, HUANG Fang, LIU Qiongying, LI Chunrong, WANG Jiyang

(Key Laboratory of Petroleum Resources Research of Chinese Academy of Sciences, Institute of Geology

and Geophysics, Chinese Academy of Sciences, Beijing 100029, China)

Abstract: Sichuan Basin, located in the western margin of Yangtze Plate, is one of the important oilgasbearing basins in China. The basin is in the passive continental margin stage with rift in SinianOrdovician. The tectonothermal evolution of basin was simulated by a geodynamical method in the lithospheric scale, and the thermal history of Early Paleozoic was obtained in order to provide important thermal parameters for assessment of hydrocarbon generation of basin. The tectonic subsidence of basin was firstly calculated by backstripping technique to provide objective function for the tectonothermal modeling; secondly, based on twodimensional multiphase extensional model, three episode extensional coefficients were estimated through fitting with the tectonic subsidences of Late Sinian, Cambrian and Ordovician in order to reveal the evolution of lithospheric base and temperature, as well as the basal heat flow. The modeling results show that the thermal disturbance, which is induced due to lithospheric extension and upwelling of asthenosphere, increases the basal heat flow in Late Sinian, and the effects are high in the northwest and southwest of basin and little in the northeast; the thermal disturbance weakens in Cambrian and disappears gradually in Ordovician, and consequently the basal heat flow decreases slowly; the basal heat flow of basin is still 5259 mW·m-2 in Early Paleozoic.

Key words: tectonothermal evolution; multiphase extensional model; Early Paleozoic; basal heat flow; lithospheric scale; numerical modeling; Sichuan Basin

0引言

盆地?zé)釟v史控制著油氣的生成、運(yùn)移、聚集以及保存等過程，是含油氣盆地分析的重要環(huán)節(jié)。熱歷史的恢復(fù)可以利用巖石圈尺度的構(gòu)造熱演化方法或盆地尺度的古溫標(biāo)方法［15］進(jìn)行。四川盆地現(xiàn)今大地?zé)崃髦灯骄鶠?3 mW·m-2,具有典型克拉通型盆地中低熱流特征［6］。近年來，許多學(xué)者對四川盆地的熱歷史恢復(fù)作了很多工作［716］，研究結(jié)果表明早二疊世—中三疊世是盆地?zé)嵫莼闹匾獣r(shí)期，其間盆地古熱流達(dá)到了其歷史最高值。傳統(tǒng)古溫標(biāo)方法由于無法恢復(fù)盆地達(dá)到最高古地溫以前的熱歷史，因而在四川盆地古生代熱歷史研究中受到局限。構(gòu)造熱演化模擬可以有效補(bǔ)充古地溫方法在該盆地應(yīng)用的局限性，填補(bǔ)該盆地早期熱歷史研究的空白。構(gòu)造熱演化模擬作為研究沉積盆地的重要手段之一，與古溫標(biāo)方法不同的是，構(gòu)造熱演化模型依賴于盆地成因類型。它必須建立在盆地成因機(jī)制的地質(zhì)地球物理模型基礎(chǔ)之上。

位于揚(yáng)子克拉通的四川盆地是一個(gè)大型古生代—中新生代海相陸相疊合盆地,蘊(yùn)含著豐富的油氣資源［1722］。它經(jīng)歷了中—晚元古代揚(yáng)子地臺基底形成階段、震旦紀(jì)—中三疊世被動大陸邊緣階段、晚三疊世盆山轉(zhuǎn)換與前陸盆地形成演化階段、侏羅紀(jì)—第四紀(jì)前陸盆地沉積構(gòu)造演化階段。其基本性質(zhì)是多旋回疊合構(gòu)造改造型盆地［23］。震旦紀(jì)開始的伸展作用在中國南方是區(qū)域性的［24］。揚(yáng)子克拉通在震旦紀(jì)—早奧陶世處于裂陷特征的被動大陸邊緣階段。盆地內(nèi)大型構(gòu)造圈閉主要發(fā)育古生代—中生代烴源巖，形成多套生儲蓋組合，是重要的油氣生、儲場所，因此，對古生代熱歷史的研究迫在眉睫。筆者擬將多期拉張模型應(yīng)用到四川盆地早古生代巖石圈拉張期(或稱為伸展期)的熱歷史研究中，利用地球動力學(xué)方法在巖石圈尺度探討盆地晚震旦世—奧陶紀(jì)構(gòu)造熱演化特征，為盆地生烴狀態(tài)、生烴期次等研究提供熱參數(shù)。

1模擬方法

本文采用的二維多期拉張模型［2528］是建立在巖石圈尺度，采用正演的方法，通過求解二維熱傳導(dǎo)方程，模擬盆地在形成演化過程中構(gòu)造位移發(fā)生變化的同時(shí)，溫度場和熱流在時(shí)間和空間上的演化歷史。研究手段是二維有限元方法，在拉格朗日坐標(biāo)系下,通過網(wǎng)格節(jié)點(diǎn)位移描述模型(巖石圈、盆地)的構(gòu)造形變、節(jié)點(diǎn)溫度描述溫度場的演變,從而再現(xiàn)盆地在拉張演化過程中的構(gòu)造和熱演化史。

在時(shí)間t=0時(shí)，初始巖石圈拉張，在橫向上不同地區(qū)拉張系數(shù)不同，巖石圈減薄程度不同，因均衡補(bǔ)償引起的初始沉降也不同。由于巖石圈減薄，熱軟流圈被動上拱，引起熱擾動，隨著時(shí)間推移，熱擾動逐漸解體，引起熱沉降［29］。在t1時(shí)刻，沒有完全恢復(fù)至熱平衡狀態(tài)的巖石圈再次拉張，進(jìn)一步減薄。第二次拉張巖石圈的初始溫度場為前一期拉張結(jié)束時(shí)的溫度場。溫度場的變化滿足二維瞬態(tài)熱傳導(dǎo)方程

ρcT t-(2KT 2x2+2KT y2)=Q(1)

式中：T為溫度；K為熱導(dǎo)率；ρ為密度；c為比熱容；t為時(shí)間；Q為熱流。

該模型忽略了沉積的影響，因此，模型計(jì)算的表面熱流為基底熱流。模型假定上、下邊界溫度始終保持不變，分別為0 ℃和1 330 ℃［29］；側(cè)邊界為絕熱邊界；放射性元素生熱集中在初始上地殼10 km范圍內(nèi)，生熱率為2.8 μW·m-3，從而使得地殼熱流為28 mW·m-2 ［30］；下地殼、地幔沒有放射性熱源。模型參數(shù)見表1［1,2930］。

表1模型參數(shù)

Tab.1Modeling Parameters

參數(shù)名稱 參數(shù)取值

原始巖石圈厚度/km 125

原始地殼厚度/km 35

0 ℃地幔物質(zhì)密度/(kg·m-3) 3 330

0 ℃地殼物質(zhì)密度/(kg·m-3) 2 800

巖石圈底部溫度/℃ 1 330

地殼巖石熱導(dǎo)率/(W·mK-1) 3.1

原始上地殼10 km巖石生熱率/(μW·m-3) 2.8

下地殼巖石熱導(dǎo)率/(W·mK-1) 2.6

熱膨脹系數(shù)/K-1 3.28×10-5

地幔巖石熱導(dǎo)率/(W·mK-1) 2.9

沉積盆地構(gòu)造熱演化模擬中，拉張系數(shù)是反映巖石圈拉張演化的重要參數(shù)。拉張系數(shù)β一般定義為初始地殼厚度與拉張后地殼厚度之比。對于只經(jīng)歷一次拉張的盆地而言，拉張后的地殼厚度即現(xiàn)今地殼厚度，很容易求得β。然而，對于經(jīng)歷多期拉張的古老盆地(如古生代的四川盆地)而言，當(dāng)時(shí)的地殼厚度很難確定，那么各期的拉張系數(shù)就很難用簡單的公式求得。另外，沉積盆地由于拉張而引起巖石圈減薄和初始沉降，同時(shí)引起溫度場的變化。隨著時(shí)間的推移，溫度場的變化又引起熱沉降。構(gòu)造沉降和溫度場演化是相互聯(lián)系的，因此，拉張系數(shù)的計(jì)算不能忽略溫度場的影響，應(yīng)放在構(gòu)造熱演化模擬中求取。這里采用非瞬時(shí)或有限時(shí)(即拉張?jiān)谝欢〞r(shí)間內(nèi)完成)多期拉張模型來模擬沉積盆地構(gòu)造熱演化，應(yīng)用迭代法通過擬合構(gòu)造沉降量來求取各期的拉張系數(shù)［25］。

2模擬結(jié)果

筆者選擇了8條穿越四川盆地的剖面(位置見圖1)，利用二維多期拉張模型對各剖面分別進(jìn)行巖石圈尺度的構(gòu)造熱演化模擬。在構(gòu)造熱演化模擬之前需要利用回剝技術(shù)恢復(fù)盆地的沉積埋藏史和構(gòu)造沉降史來作為模擬的目標(biāo)函數(shù)。由于這里采用的是一維回剝技術(shù)，因此需要在剖面上每隔一段距離選取鉆井或人工井來獲取構(gòu)造沉降數(shù)據(jù)。

圖1四川盆地構(gòu)造簡圖及模擬剖面和井的位置

Fig.1Tectonic Sketch of Sichun Basin and Positions of Modeling Profiles and Wells

為了詳盡地描述模擬過程和結(jié)果，這里以位于川中地區(qū)及川東南地區(qū)4口鉆井(位置見圖1)為例進(jìn)行剖析。它們分別是GK1、NvJ、DS1及Lin1井，鉆井地層數(shù)據(jù)見表

2［31］。沉積盆地的埋藏史是指盆地中某一沉積單元自沉積開始至今的沉積過程，即是經(jīng)過堆積、壓實(shí)、抬升及剝蝕的動力學(xué)演化過程。一般采用壓實(shí)校正的方法來恢復(fù)其沉積埋藏史。壓實(shí)校正是把某一地層單元的實(shí)測厚度恢復(fù)到沉積時(shí)或埋藏過程中某一時(shí)期的厚度。壓實(shí)主要是上覆地層質(zhì)量使地層內(nèi)流體排出,孔隙度減小，因此，校正前應(yīng)得到盆地正常壓實(shí)條件下孔隙度與埋深的關(guān)系。骨架密度(ρsg)為2 680 kg·m-3，孔隙度和埋深的一般關(guān)系為［32］

φ= φ0e-ez (2)

式中：φ為孔隙度；φ0為地表最大孔隙度，采用φ0=05；z為埋深；e為壓實(shí)系數(shù)［33］，采用e=04。

然而，除了NvJ井，其余3口鉆井都沒有鉆穿燈影組。區(qū)域?qū)Ρ确治霰砻鳎?5,34］，川東南地區(qū)燈影組巖性、厚度較為穩(wěn)定，均為局限臺地白云巖、藻白云巖等，厚度一般為700~900 m，因此，Lin1、GK1井燈影組模擬厚度暫取700 m。利用回剝技術(shù)可以得到模擬井晚震旦世—早中奧陶世時(shí)期沉積埋藏史和構(gòu)造沉降史［圖2(a)、(b)］。結(jié)果顯示：盆地在晚震旦世經(jīng)歷了快速沉降，構(gòu)造沉降量(空盆沉降)達(dá)到600 m［圖2(b)］，總沉降量超過1 700 m；到了寒武紀(jì)，沉降速率有所降低，但構(gòu)造沉降量并不小，甚至超過震旦紀(jì)的構(gòu)造沉降，此時(shí)盆地的沉降量已接近3 500 m；到了奧陶紀(jì)，無論是構(gòu)造沉降量還是沉降速率都進(jìn)一步降低。由于數(shù)據(jù)量龐大，剖面上其他人工井這里不再一一圖示。

在構(gòu)造沉降史研究基礎(chǔ)之上，利用二維多期拉張模型即可分別模擬各剖面的構(gòu)造熱演化歷史。巖石圈拉張模式為非瞬時(shí)(有限時(shí))，每期拉張速率為勻減速模式

［26］。通過分別與剖面3個(gè)時(shí)期構(gòu)造沉降量的擬合，可以得到巖石圈3期拉張演化階段的拉張系數(shù)。從表3可以看出：4口井在晚震旦世

表2模擬鉆井早古生代地層數(shù)據(jù)

Tab.2Stratigraphic Data of Modeling

Wells in Early Paleozoic

地層層序

系 統(tǒng) 組 代號 底界年

齡/Ma 底界深度/m

Lin1井 DS1井 GK1井 NvJ井

志

留

系

奧

陶

系

寒

武

系

震旦

系 中下統(tǒng)

下

統(tǒng)

上

統(tǒng)

中

統(tǒng)

下

統(tǒng)

中上統(tǒng)

中

統(tǒng)

下

統(tǒng)

上統(tǒng) 韓家店組 S12h 400.0 458.0

石牛欄組 S1sh631.0 1 375.8

龍馬溪組 S1l 443.7 773.0 1 520.0

五峰組 O3w777.0 1 523.5

澗草溝組 O3j782.0 1 529.0

寶塔組 O2b 460.9 810.0 1 559.2

十字鋪組 O2sh 460.9 823.0 1 559.2

牯牛潭組 O2gh 1 570.0

湄潭組 O1m1 055.0 1 785.5

紅花園組 O1h 478.6 1 087.0 1 832.5

桐梓組 O1t 488.3 1 224.0 1 980.0 4 396.0 4 557.0

婁山關(guān)組 ∈23l 508.0 1 828.0 2 655.0 4 622.0 4 898.0

石冷水組 ∈2sh1 929.0 2 760.0

陡坡寺組 ∈2d 510.0 1 970.0 2 803.0 4 710.0

清虛洞組 ∈1q2 140.0 2 997.0

金頂山組 ∈1j2 290.0 3 130.0 4 762.0

明心寺組 ∈1m2 415.0 3 302.5 4 875.0 5 110.0

牛蹄塘組 ∈1n 542.0 2 586.0 3 494.0 4 992.0 5 201.0

燈影組 Z2dn 551.0 2 910.0 4 610.0 5 480.0 6 022.0

注：除了NvJ井，其余3口井都沒有鉆穿燈影組；NvJ和GK1井的志留系和大部分奧陶系地層缺失。

圖2模擬井晚震旦世—早中奧陶世時(shí)期沉積埋藏史和構(gòu)造沉降史

Fig.2Burial History and Tectonic Subsidence of Modeling Wells from Late Sinian to EarlyMiddle Ordovician

拉張系數(shù)最大，在1121~1201之間，其中DS1井拉張量最大；到了寒武紀(jì)，拉張系數(shù)普遍降低，介于1.031~1.097，其中Lin1井拉張量最大；到了早奧陶世，拉張系數(shù)已非常低，盆地基本上處于熱沉降的坳陷階段。

表3典型模擬井的拉張系數(shù)

Tab.3Extensional Coefficients of the

Typical Modeling Wells

地質(zhì)時(shí)代 Lin1井 DS1井 GK1井 NvJ井

晚震旦世 1.136 1.201 1.138 1.145

寒武紀(jì) 1.080 1.050 1.015 1.019

早中奧陶世 1.005

根據(jù)拉張系數(shù)可以得到巖石圈底界和溫度場的演化以及基底熱流隨時(shí)間的演化(圖3、4)。模擬結(jié)果顯示，盆地基底熱流在晚震旦世—早奧陶世時(shí)期巖石圈拉張演化過程中始終在52~59 mW·m-2范圍內(nèi)。該值要小于早二疊世—中三疊世時(shí)期盆地在區(qū)域巖石圈拉張和峨眉山地幔柱共同作用下所達(dá)到的最高古熱流［8，1011］。這是因?yàn)槔瓘埩?拉張系數(shù))不是很大，而且拉張持續(xù)時(shí)間較長，巖石圈地幔上涌造成的熱擾動在拉張過程中已逐步消減，無法積累足夠大的熱異常。在此期間，巖石圈雖有減薄但很有限，底界上升幅度不是很大(圖4)。

綜合8條剖面的模擬結(jié)果即可得到基底熱流在全盆地的平面分布(圖5~7)。震旦紀(jì)時(shí)期，盆地在巖石圈拉張作用下，基底熱流略有升高，其中高值主要分布在盆地西北與西南，均超過58 mW·m-2。而川東北受到巖石圈拉張作用影響很小，基底熱流普遍低于56 mW·m-2。寒武紀(jì)—奧陶紀(jì)巖石圈拉張?jiān)斐傻臒釘_動已基本消失，基底熱流呈緩慢下降趨勢，且下降幅度很小。全盆地基底熱流分布相對均勻，寒武紀(jì)基底熱流為54~55 mW·m-2，盆地中川西和川西北熱流值相對較高，川東和川東南相對較低；而奧陶紀(jì)則為53~54 mW·m-2，整體趨勢呈現(xiàn)川西地區(qū)熱流較高，且由川西向川東熱流值逐漸降低。

圖3四川盆地晚震旦世—早中奧陶世時(shí)期基底熱流的演化

Fig.3Evolution of Basal Heat Flow in Sichuan Basin

from Late Sinian to EarlyMiddle Ordovician

圖4巖石圈底界及溫度場的演化

Fig.4Evolution of Lithospheric Base and Temperature Field

圖5四川盆地晚震旦世基底熱流分布

Fig.5Basal Heat Flow Distribution of Sichuan Basin in Late Sinian

圖6四川盆地寒武紀(jì)基底熱流分布

Fig.6Basal Heat Flow Distribution of Sichuan Basin in Cambrian

圖7四川盆地奧陶紀(jì)基底熱流分布

Fig.7Basal Heat Flow Distribution of Sichuan Basin in Ordovician

3結(jié)語

(1)在巖石圈拉張減薄的深部動力學(xué)機(jī)制作用下，晚震旦世四川盆地軟流圈上涌形成熱擾動，震旦紀(jì)時(shí)期基底熱流值有所升高?？傮w上，巖石圈拉張程度較弱，拉張系數(shù)小于1.3。由于拉張系數(shù)較小，巖石圈的減薄量有限，受到的熱擾動不大，震旦紀(jì)基底熱流最大約59 mW·m-2，其中熱流高值主要分布在盆地西北與西南，而川東北受到拉張作用的影響最小。

(2)盡管拉張作用在寒武紀(jì)仍持續(xù)著，但強(qiáng)度較上一時(shí)期還弱，基底熱流為54~55 mW·m-2。至奧陶紀(jì)，熱擾動基本消失，盆地?zé)崃髦党示徛陆第厔荩胰璧鼗谉崃鞣植枷鄬鶆?，?3~54 mW·m-2。

(3)盆地基底熱流在晚震旦世—早奧陶世時(shí)期巖石圈拉張演化的過程中變化不是很大，始終在52~59 mW·m-2范圍內(nèi)。該值要小于早二疊世—中三疊世時(shí)期盆地在區(qū)域巖石圈拉張和峨眉山地幔柱共同作用下所達(dá)到的最高古熱流。

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MA Yongsheng.Marine Petroleum Exploration in China［M］.Beijing:Geological Publishing House,2007.

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HE Lijuan,XIONG Liangping,WANG Jiyang,et al.Calculation of Extension Coefficients in Modeling Multiple Extensional Basins［J］.Chinese Science Bulletin,1995,40(24):22612263.

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HE Lijuan.Multiple Tectonothermal Modeling of Liaohe Basin in the Cenozoic［J］.Chinese Journal of Geophysics,1999,42(1):6268.

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TANG Qingyan,ZHANG Mingjie, ZHANG Tongwei,et al.A Review on Pyrolysis Experimentation on Hydrocarbon Generation［J］.Journal of Southwest Petroleum University:Science and Technology Edition,2013,35(1):5262.

［29］MCKENZIE D.Some Remarks on the Development of Sedimentary Basins［J］.Earth and Planetary Science Letters,1978,40(1):2532.

［30］郭正吾，鄧康齡，韓永輝，等.四川盆地形成與演化［M］.北京：地質(zhì)出版社,1996.

GUO Zhengwu,DENG Kangling,HAN Yonghui,et al.Formation and Evolution of the Sichuan Basin［M］.Beijing:Geological Publishing House,1996.

［31］孫瑋.四川盆地元古宇—下古生界天然氣藏形成過程和機(jī)理研究［D］.成都:成都理工大學(xué),2008.

SUN Wei.The Research on the Formation Process and Mechanism of Gas Pools in Proterozoic to Low Paleozoic Erathem,Sichuan Basin［D］.Chengdu:Chengdu University of Technology,2008.

［32］ALLEN P A,ALLEN J R.Basin Analysis:Principles and Applications［M］.3rd ed.London:WileyBlackwell,2013.

［33］SCLATER J G,CHRISTIE P A F.Continental Stretching:An Explanation of the PostMidCretaceous Subsidence of the Central North Sea Basin［J］.Journal of Geophysical Research:Solid Earth,1980,85(B7):37113739.

［34］劉若冰,田景春,黃勇,等.川東南震旦系燈影組白云巖與志留系石牛欄組灰?guī)r儲層特征［J］.成都理工大學(xué)學(xué)報(bào):自然科學(xué)版,2007,34(3):245250.

LIU Ruobing,TIAN Jingchun,HUANG Yong,et al.Characteristics of the Carbonate Rock Reservoir of the Upper Sinian Dengying Formation and the Lower Silurian Shiniulan Formation in the Southeast of Sichuan,China［J］.Journal of Chengdu University of Technology:Science and Technology Edition,2007,34(3):245250.