煤礦開采外文翻譯---煤形成環(huán)境及其與斯蒂芬期聚煤盆地的構(gòu)造活動

1、<p><b>　　附錄1 </b></p><p>　　煤形成環(huán)境及其與斯蒂芬期聚煤盆地的構(gòu)造活動</p><p>　　Dennis L. Nielson Gamma</p><p>　　法國南部的塞文山脈煤盆地位于東南部法國山岳的中心，以前的研究主要針對于它的地層，巖石學(xué)，煤的化學(xué)成份，煤炭巖石學(xué)和地質(zhì)構(gòu)造。這項(xiàng)研究的目標(biāo)將強(qiáng)調(diào)位

2、于山脈之間的法國山岳的中心盆地在構(gòu)造形式和煤炭形成晚期沉淀環(huán)境之間的關(guān)系, 在中國類似第三紀(jì)煤炭盆地形成，煤炭縫厚度和范圍基本上由早期的構(gòu)造活動控制。 </p><p>　　1.塞文山脈煤炭盆地區(qū)域性的結(jié)構(gòu)</p><p>　　盆地北部的煤系露頭厚度達(dá)到2500米。盆地南部的覆蓋了一系列的中世紀(jì)地層.兩個主要的斷層中間夾有50 公里寬煤盆地。 </p><p>　　

3、盆地被劃分成西部(研究區(qū)域)和 一個東部次級盆地。 西部次級盆地在這項(xiàng)調(diào)查研究中被劃分為三個部分，從北到南分別為：地塹，由于斷層而形成的鄂圖曼地壘和洛杉磯巨大的深谷地塹。 </p><p>　　本文重點(diǎn)研究位于塞文山脈盆地西北部的煤的特征和范圍和碎屑物的范圍，和他們的與早期的構(gòu)造活動的關(guān)系。 </p><p><b>　　2.地層學(xué)結(jié)構(gòu)</b></p>

4、<p>　　在斯蒂芬期的一系列盆地—沉積的順序由巖屑組成的巖石決定，包括：礫巖或角礫巖，粗砂巖，粉砂巖，泥巖和煤縫合線。</p><p>　　沉積的序列從底部到頂部可以分為六個地層單位地層學(xué)的結(jié)構(gòu)是除了邊緣斷層以外的各種不同沉淀的環(huán)境和他們的相互關(guān)系的分布范圍的結(jié)果。盆地腹部斷層例如： 斷層也影響了個體的地理分布和不對稱地塹的發(fā)育。大型的地塹和煤縫合線的范圍，以及早期和后期的層序都與邊緣和盆地腹部的斷層

5、有關(guān)。 重要煤層在序列的中間部分被集中。</p><p>　　3.塞文山脈煤盆地煤的層序</p><p>　　目前分析的煤的層序是以大量的地質(zhì)區(qū)域鉆芯和老的礦層補(bǔ)充日志為基礎(chǔ)。從薄的部分觀察和統(tǒng)計(jì)處理獲得的沉積學(xué)數(shù)據(jù)來完成古地理學(xué)和史前環(huán)境的解釋。有不充足的圖解數(shù)據(jù)和地層學(xué)的起源的相互作用來歸納地層層序。</p><p>　　3.1 第一階段：單位沉積物 <

6、/p><p>　　單位形成于在早期的次級盆地。主要沖積扇系統(tǒng)以洛杉磯巨大深谷地塹為中心。近扇形和中扇形的沉積由角礫巖聚結(jié)和粗砂巖控制，包含的片麻巖和石英的碎片最大直徑達(dá)到40cm。近扇形和中扇形沉積主要集中在研究區(qū)域的西部，接近維勒福爾斷層并進(jìn)一步向東延伸。巨大的扇形由沙質(zhì)和泥質(zhì)的沉積物組成。除了接近佩特努斷層，一些小扇形聚集物被沉積了下來，在東部盆地沖積扇發(fā)育不足，并且包括細(xì)顆粒的沉積，。在這個階段期間， 佩特努斷

7、層和與西部邊緣斷層一起控制了各種沉積的范圍。 </p><p>　　3.2 第二階段：理查得單位的沉積物 </p><p>　　沉積還發(fā)生在洛杉磯巨大深谷地塹，并向東部和西部延伸。扇形的沉積延伸著西部的邊緣延伸，又回到維勒福爾斷層，以減少連續(xù)沉積物的區(qū)域和厚度。巨大的沖積扇，由沙質(zhì)沉積物組成，在洛杉磯巨大深谷地塹東部和西部邊緣發(fā)育并沿著NE-SE方向加寬了。在洛杉磯巨大深谷地塹的中心，

8、沼澤在沖積扇平原前面位置開育，泥煤富集在沼澤的中央部分。泥煤富集區(qū)域下面覆蓋了單位的厚實(shí)的沖積扇聚集物。對應(yīng)的厚實(shí)煤層迅速地沿佩特努斷層向東西方向分裂，并控制了煤炭富集區(qū)域的發(fā)育。 </p><p>　　3.3第三階段：整個盆地的沉積</p><p>　　在這個階段，沉積發(fā)生在整個盆地，反映了增加的范圍和下陷的比例。沿著西部邊緣到盆地的東部邊緣沖積扇控制了南部的地塹，佩特努斷層形成了巨大的

9、扇形沉積。泥炭沼澤在扇形平原的前緣沉積下來。而泥炭的沉積物被暫時的分開，形成了一些側(cè)面變化的薄煤層。一些小型的沼澤在扇形和昌普斯村之間發(fā)育，形成了非常薄的煤層，而巨大的扇形砂質(zhì)沉積控制了北部的地塹北部盆地。</p><p>　　在拉維多地塹的北部，古地層成為沖積扇體系的標(biāo)志層，沉積物暗示了出現(xiàn)在超級盆地西部的扇形沉積，而古河流的方向暗示了三角洲向中東部遷移，也暗示了東部邊際碎屑的來源。砂質(zhì)沉積物都出現(xiàn)在巨大三角洲

10、的中部地區(qū)。沼澤在東部超級盆地的恰莫和昌普斯斷層之間的沖積扇平原上廣泛發(fā)育。在拉維多地塹的西部邊際的保羅因斷層非常活躍，從而形成了半地塹構(gòu)造。</p><p>　　在鄂圖曼地壘，大顆粒的碎屑體也發(fā)育在西部，而且向東部逐漸變薄，在地壘的東部，沉積物和砂質(zhì)沉積物形成了次級砂巖。</p><p>　　3.4 第四個階段：巨大的波美單位沉積</p><p>　　在洛杉磯巨

11、大的深谷地塹，沖積扇只發(fā)育在次級盆地的東北部分，碎屑物來源于東部，在特努和墨菲斯特?cái)鄬又g，發(fā)育了廣闊的河流沼澤體系，泥煤在洪水沖積平原被積累起來。形成了鄰近和平行于活躍的墨菲斯特?cái)鄬拥拿禾扛患瘏^(qū)域。</p><p>　　在拉維多地塹，扇體被限制在北和西部，與先的階段相比較扇體的范圍和組成物的顆粒粒度都減小了。形成的大面積的沼澤代替了沖積扇平原中的扇形砂質(zhì)沉積，從而形成了幾個煤系地層。</p>&l

12、t;p>　　在鄂圖曼地壘，沖積扇也被限制在東西部地區(qū)，并沿著鄂圖曼村發(fā)育。在東部的泥煤沼澤，發(fā)育了一些薄煤系地層。 </p><p>　　3.5 第五個階段：陸明特單位的沉積物</p><p>　　洛杉磯巨大的深谷地塹沖積扇發(fā)育在東北部邊緣，受到特努和墨菲斯特?cái)鄬拥臉?gòu)造控制，在扇體中主要由粗大的砂巖和碎石組成的，但沒有大的鵝卵石。在地塹的中央，埋藏著兩個大的富煤區(qū)域，周圍是由分選

13、良好的花崗質(zhì)砂巖組成。沼澤和花崗質(zhì)砂巖區(qū)域從西南向東北方向移動。在狹窄的墨菲斯特和帕魯貝斷層的凹陷區(qū)域，發(fā)育了一些煤系地層，每一層的平均厚度不到1米。在洛杉磯聞密得地塹，扇體的中心和附近區(qū)域主要分布在北部邊緣，沿著構(gòu)造運(yùn)動形成的保羅因和帕魯貝斷層西部邊際由扇體顆粒狀含砂沉積和次級粗糙沉積物組成。泥炭沼澤發(fā)育在中心和東部地帶，周圍是黑色魚鱗狀含鈣質(zhì)或鐵的油頁巖淺湖沉積物。沿著湖的西岸發(fā)育了一個小的完整的三角洲體系。碎屑物來自洛杉磯保羅因地

14、塹的西部邊緣。沼澤沿著淺湖的沖積平原延伸，在那里形成了薄的煤系地層，一些小型的沖積扇沿著西部邊緣發(fā)育。</p><p>　　3.6 第六個階段：理查德單位的沉積物 </p><p>　　巨大的洛杉磯深谷地塹沉積只發(fā)生在昌普斯北部，而沖蝕發(fā)生在南部，小型的沖積扇沿著東北部的邊緣發(fā)育，在其它的地區(qū)主要由粗糙的沉積物組成，與第五階段相比，泥炭沼澤和煤富集區(qū)域向東北方向移動。拉維多地塹的西部上升

15、，且沒有沉積物形成。在第五階段形成的三角形的湖變成狹長型區(qū)域并且由大顆粒的長石砂巖沉積形成。沿著西部邊緣，一個被淹沒的扇開三角洲被合并成一個中央湖。這個復(fù)合體大約有100米厚，并且表現(xiàn)為完全的反向分級的礦床。河岸由粗糙的巖石組成，在這個階段期間，當(dāng)保羅因斷層的活動減少時，卡馬斯斷層的活動卻非常頻繁，從而形成了一個向東的急傾斜的和一個向西的緩慢傾斜的半分離的地塹構(gòu)造，鄂圖曼地壘主要是由分類良好的長石砂巖沉積形成。</p>&

16、lt;p>　　在第六個階段的結(jié)束時，文塞山脈盆地的西部和北部上升而且沉積結(jié)束了。 </p><p>　　4.塞文山脈盆地的構(gòu)造活動</p><p>　　像其它的被斷開的盆地一樣，盆地腹部的強(qiáng)度和樣式的變化程度以及塞文山脈盆地邊緣斷層影響和控制成煤環(huán)境。以洛杉磯巨大的深谷地塹北部的盆地做為的例子和基礎(chǔ)來研究洛杉磯巨大的深谷地塹南部盆地的斷層，我們談?wù)摻Y(jié)構(gòu)框架的演變， 盆地腹部的構(gòu)造運(yùn)動

17、和它對沉積物變化特征及煤的形成的影響。</p><p>　　可以看到在中早期的斯蒂芬期，換言之，也就是在斯蒂芬期的第三沉積階段和第四個盛大波美單位在盆地演變期間，在西部邊緣的防水?dāng)鄬拥膭×疫\(yùn)并且控制了粗糙碎屑體的空間分布。在東部的邊緣沒有斷層發(fā)育。盆地的構(gòu)造是一個半地塹形式，這個含有砂巖和聚集的粗糙的碎屑沉積物的南部斷層發(fā)育。</p><p>　　這種粗糙的碎屑體呈透鏡狀，使斷層加厚并且與

18、維班克斷層平行所以顯然它受到斷層的控制。這種大塊的粗糙碎屑體由粗糙變?yōu)楣饣?，這種巖石從沉積的砂巖變成粗粉砂巖、泥巖和煤層。這個斷層的北部斷盤是由粗砂巖，粉砂巖，泥巖和煤層組成。在斯蒂芬期的中晚期，也就是第五個沉積階段，扇體主要分布在變成了拉維多地塹的北部邊緣，并且被保羅因和卡馬斯斷層貫穿。在這個時期，東部和西部的邊緣斷層控制著地層結(jié)構(gòu)并形成了結(jié)構(gòu)上對稱的拉維多地塹。在斯蒂芬期的晚期，也就是第六個沉積階段，由粗糙的沉積物形成的扇形三角洲的

19、圓形突出部分在卡馬斯斷層和斯諾丁斷層區(qū)域有良好的發(fā)育,古老河流方向暗示了扇形三角洲的葉部來源于東部，在這個階段，卡馬斯斷層北部邊緣構(gòu)造運(yùn)動劇烈，而保羅因斷層西部的構(gòu)造運(yùn)動緩慢，從而使拉維多地塹東部下滑，西部劇烈下滑的半地塹。</p><p><b>　　5.結(jié)論 </b></p><p>　　在上文中對斯蒂芬期煤炭盆地的詳細(xì)的結(jié)構(gòu)和沉積地層的研究解釋了盆地的環(huán)境演變并

20、且敘述了煤炭的形成過程。在斯蒂芬期塞文山脈盆地的東北部地區(qū)，泥煤沼澤形成了在沖積扇系統(tǒng)的末端部分，并被限制在與邊緣斷層有關(guān)的盆地邊緣。</p><p>　　由于劇烈的盆地外的構(gòu)造運(yùn)動導(dǎo)致了輕微的下陷和后來碎屑物的快速的填充，泥煤發(fā)展和不保護(hù)開采是罕見的。構(gòu)造運(yùn)動的暫時停止能使泥炭發(fā)育，并能使沉積物廣泛的覆蓋河系。 </p><p>　　在洛杉磯巨大的深谷地塹，煤炭形成環(huán)境經(jīng)歷了從早期和晚期

21、的斯蒂芬期階段沼澤沖積扇系統(tǒng)到進(jìn)入中期的沼澤沖積湖上的系統(tǒng)階段，連接與對應(yīng)盆地發(fā)展和消失的三個構(gòu)造階段的演變。 </p><p>　　煤炭沼澤范圍轉(zhuǎn)變，富集煤炭區(qū)域和沖積層是由盆地腹部和邊緣斷層控制的。沖積扇聚成團(tuán)身體發(fā)行和極限準(zhǔn)許容易地重建少量的缺點(diǎn)的活動和提高來源地區(qū)。</p><p>　　另一方面，碎屑物和沉積的有機(jī)物之間線性和嚴(yán)格的限制暗示了盆地腹部斷層活動的改造。從沉積特征推斷的

22、構(gòu)造的說明與以構(gòu)造分析為基礎(chǔ)的構(gòu)造演變是一致的，并且通過盆地的空間和時間推斷的古應(yīng)力場和他變化。</p><p><b>　　附錄2</b></p><p>　　Coal forming environments and their relationship to tectonic activity in the Cevennes Stephanian coal ba

23、sin</p><p>　　Dennis L. Nielson Gamma</p><p>　　The Stephanian C6vennes coal basin is located in the southeastern part of the French Massif centra1．Previous </p><p>　　studies focused

24、on its stratigraphy，sedimentary petrology，coal chemistry ， coal petrology and structural geology.</p><p>　　The aim of this study is to highlight the relationships between the tectonic patterns and the sedime

25、ntary environments of coal formations in the late Hercynian interm ontane basins of the Massif central in France , resemble the Tertiary coal basins in China where the occurrence, distribution and the thickness of the co

26、al seams are essentially controlled by early tectonic activity． </p><p>　　1.Regional framework of Cevennes coal basin </p><p>　　The coal measures are up to 2500 m thick and outcrop in the northe

27、rn part of the basin．Mesozoic strata cover the stephanian series in the southern basin．The two main faults Villefort and Crvennes borde the 50km2 wide coal basin．The basin is divided into a western (study area)and an eas

28、tern subbasins．The western subbasin was investigated in this study is divided with three areas，respectively from north to south：La Vernarede graben， Portes horst and La Grand—Combe graben，by the Paulin and Chamarit</p

29、><p>　　This paper focuses on the characteristics and distribution of the coal and clastics distribution in the north—western part of the Crvennes coal basin，their palaeoenVimnmentale setting and their relations

30、hips with the early tectonic activity． </p><p>　　2.Stratigraphic famework </p><p>　　The Stephanian series of the basin—fill sequence are dominated by detrital rocks including conglomerates or br

31、eccias，coarse and fine grained sandstones，sihstones，mudstones and coal seams The depositional sequence canbe divided into six lithostratigraphic units from bottom to top ：① Strriles inf．de La ForSt unit；② Ricard unit； ③

32、Strriles sup．de La Foret unit； ④ Grand—Baume unit； ⑤ Luminieres unit；⑥ Champclauson unit．The stratigraphic framework is a result of the distribution of various deposition</p><p>　　3.Coal bearing sequences in

33、 the Cevennes basin </p><p>　　The analysis of coal bearing sequences presented here is based on a large amount of geologiical field sections drill cores and well logs complemented by sections in ancient min

34、ing galeries．The paleogeographical and paleoen vironmental interpretations were performed using farther inform ation derived from thin section observations and statistical processing of sedimentological data．Correlations

35、 within the basin are discussed using poor biostrati graphical data and genetic stratigraphy induced se</p><p>　　3．1 The first stage：deposition of the Strriles inf．de la Foret unit </p><p>　　Th

36、e Strriles inf．de la Forget unit form ed at the beginning of the opening of the sub-basin．Mainly alluvial fan systems started at the center of the La Grand-Combe graben．The near-fan and middle-fan deposits are dominated

37、by breccias，conglomerates and coarse—grained sandstones，containing gneiss and quartz fragments with a max．diameter up to 40 cm．Near-and middle—fan mainly developed in the west part of the study area，close to the marginal

38、 Villefort fault and advanced eastward．The far-fan was dom</p><p>　　3．2 The second stage：deposition of the Ricard unit </p><p>　　The deposition still occurred in the La Grand-Combe graben，but e

39、xtended both towards eastwards and west-mentward．The fan conglomerate，well-developed along the western margin，drew back to the Villefort fault，with decreasing of both deposition area and thickness of the series．The far—f

40、an，composed of sandy sediments，developed at the eastern and western margins of the La Grand-Combe graben and widened along a NE—SE direction．In the central part of La Grand-Combe graben，swamps developed in fore—fan p<

41、/p><p>　　3．3 The third stage：deposition of the Strriles sup </p><p>　　During this stage，deposition occurred throughout the whole basin，reflecting the increased extent and rate of subsidence．Alluvi

42、al fans dominated in the southern La Grand-Combe graben，from the western bo rder and along the eastern margin of the basin，where large fan conglomerates were controlled by the Peyraube fault．Peat swamps settled in the fo

43、refan plain．The accumulation of peat，however，was episodically interrupted，resulting in the formation of several thin coal seams with lateral variations in</p><p>　　To the north in the La Vernarede graben，dis

44、tinct lithostratigraphic units are recognizable as part of alluvial fan systems．Breccias and conglomerates indicate the near—and middle-fan facies occur in the western part of the sub- basin．The paleocurrent directions i

45、ndicate that the fans moved towards the central and eastern parts，implying a source of clastics in the western margin．Sandy sediments are representative of the far-fan central part．Swamps developed acrl0ss alluvial fan p

46、lains between the</p><p>　　In the Portes horst,Cofirse-grained clastic bodies also developed in the westem part，and thined eastwards．To the east of Portes village．conglomerates and sandy conglomerates domina

47、ted with subordinate sandstones．</p><p>　　3．4 The fourth stage：deposition of the Grand-Baume unit</p><p>　　In the La Grand-Combe grabent the alluvial fans are confined to the northeastern part o

48、f the sub-basin，with clastics originating from the east.Between the Thrrond and Malperthus faults, extensive river／swamp systems developed．Peat mainly accumulated in alluvial flood plains．The coal enrichment zones formed

49、 close to and parallel to the active Malperthus fault．</p><p>　　In the La Vemarede graben，the fan bodies are confined to the northern and western parts，while their extent and the grain size of their constitu

50、ent were reduced，in comparision with the preceding stage． Widely developed swamps mainly replaced far-fan sandy sediments over the alluvial fan plains，leading to a few mineable coal seams． </p><p>　　In the P

51、ortes horst，alluvial fan bodies are also confined to the northwestem part，and far-fans developed close to the Portes village．In the peat swamps to the east，some minor thin seams developed． </p><p>　　3．5 The

52、 fifth stage：deposition of the Luminieres unit </p><p>　　In the La Grand-Combe graben alluvial fan bodies，tectonically controlled by the Th6rond and the Malperthus faults，developed at the northeastem margin.

53、 Conglomerates and gravelly coarse-grained sandstones without large pebbles are dominant in these bodies．In the central part of the graben，swamps with two coal enrichment zones are dominant，surrounded by well sorted arko

54、ses．The swamp and arkose areas(① and② in moved from the southwest to the northeast．In the narrow trough between the Malperthus and</p><p>　　The western margin of the Portes horst was uplifted and emerged，whi

55、le sandy sedimentation dominated in the central part，and wide swamps in the eastern part，leading to the formation of several thin mineable coal seams． Small alluvial fan groups grew along the eastern margin． </p>

56、<p>　　3．6 The sixth stage：deposition of the Ricard unit </p><p>　　In the La Grand-Combe graben deposition occurred only north to Champclauson．While erosion took place to the south．Small alluvial fans d

57、eveloped along the northeastern margin，and fine grained sediments dominated the other depositional regions．Compared with the fifth stage，peatswamps and coal enrichment zones shifted towards the northeast． </p><

58、;p>　　The western part of the La Vemarede graben uplifted and no deposits form ed．The triangular shape of the lake formed in the fifth stage changed into an elongated area in which fine-grained arkoses were deposited．A

59、long the western margin，a submerged fan-delta complex prograded into the central lake．This complex is about 100 m thick，and shows a complete reverse-graded bedding．Th e coarser part is composed of coarse．grained sandston

60、es，gravel-bearing coarse-grained sandstones and rounded conglomerate</p><p>　　At the end of the sixth stage，the north-western part of the Crvennes basin uplifted and Stephanian deposition ended </p>&

61、lt;p>　　4.Tectonic activity of C6vennes basin </p><p>　　As in other faulted basin．the variations in the intensity and style of the intrabasinal and marginal faults of the Crvennes basin influenced and cont

62、rolled the coa1．forming envomments. Taking the La Vemarede graben in the northern basin as an example and based on the study of faults in the La Grand-Combe graben in the southern basin，farther we discuss the evolution o

63、f structural framework，the activity of the intrabasin faults and their iniluence on the sedimentary regime and formation of coa1． </p><p>　　It can be seen that during early-middle Stephanian the third deposi

64、tion stage of the Stieriles sup．de La Foret unit and the fourth deposition stage of the Grand-Baume unit during basin evolution，the Paulin fault at the western margin moved intensely and controlled the spatial distributi

65、on of the coarse clastic bodies． At the eastern margin no fault was developed．The structural framework of the basin is a half-graben pattern，with W erbrouck fault having a strike of N125。．dip of N35。and dip angle </p&

66、gt;<p>　　At the end of middle Stephanian and during late Stephanian，i．e．the fifth deposition stage of the Luminieres unit，the near．a(chǎn)nd middle．fan bodies were distributed on the northern margin of the La Vemarede g

67、raben，where the Paulin fault and the Comas fault intersected．During this stage，both east and west marginal faults controlled the stratigraphic framework and resulted in the nearly symmetrical structural framework in the

68、La Vemarede graben．</p><p>　　At the end of Stephanian ，i． e．the sixth deposition of the Champclauson unit，fan-delta lobes constructed by coarse sediments were well developed at the region where the Comas fau

69、lt and the The rond fault．The paleocurrent directions indicate that the fan-delta lobe came from the east．During this stage，the eastern marginal Comas fault moved intensely and the western Paulin fault consumed，resulting

70、 in the transform ation of the stmctural framework of the La Vemarede graben into half-graben with a f</p><p>　　5.Conclusions </p><p>　　The detailed structural and sedimentological study of the

71、Stephanian Cevennes coal basin revealed the environmental evolution of the basin and placed the coal forming processes in this context．In the northeastern domain of the Stephanian Cevennes basin，peat swamps developed ove

72、r the distal part of alluvial fan systems，confined to the basin border in relation to margin faults．Because of relatively intense extra-and-intrabasinal tectonic movements inducing differential subsidence and subsequent

73、ra</p><p>　　In the La Grand-Combe graben，coal-forming environments underwent an evolution from swamps over alluvial fan systems in the early and late Stephanian stages to swamps over alluvial-lacustrine syst

74、ems in the middle stage，linked to corresponding three tectonic stages of the basin development and extinction． </p><p>　　The distribution and shifting of peat swamps，coal enrichment zones and alluvial deposi

75、ts were controlled by intrabasinal and marginal faults．The distribution and limits of alluvial fan conglomerate bodies allow to reconstruct easily both the activity of the marginal faults and uplifting of the source regi