華北克拉通西部地塊
華北克拉通西部地塊是一個古微板塊,主要由新太古代和古元古代基岩構成,部分地區被寒武紀至新生代的噴出岩和沉積岩覆蓋。[2]它是華北克拉通兩個子陸塊之一。西部地塊的便捷在不同模型中略有不同,但其形狀和面積是相似的。廣泛的共識是,西部陸塊覆蓋了中國中東部大部分地區。[1][3][4][5][6][7]
![](http://upload.wikimedia.org/wikipedia/commons/thumb/2/23/The_location_of_Western_Block_of_North_China_Craton.jpg/363px-The_location_of_Western_Block_of_North_China_Craton.jpg)
西部地塊存在火成岩、沉積岩和變質岩。最古老的地質記錄是內蒙古西烏蘭布朗發現的27億年前形成的深成火成岩。[8]最年輕的岩石是見於河北三義堂的造山帶噴出火成岩,形成於2300萬年前。[9]沉積岩主要分佈在西部區塊南部的鄂爾多斯盆地。[10]變質岩的出露大多在地塊北部。
西部地塊的構造環境和演變存在爭議。有各種模型假設該區塊的分區和構造史,它們通常相互矛盾。然而,大多數模型都同意存在一個古元古代造山帶,東西方向橫穿西部地塊,儘管有不同的名稱。[10]
由於西部地塊的地質事件始於前寒武紀,當時超過80%的現有大陸地殼體積已經形成了,[11][12][13]所以可以通過西部地塊的地質記錄,研究複雜的地質演變和早期構造史。[14][15]
岩石
編輯前寒武紀基岩(46–5.39億年前)
編輯太古宙岩石(40–25億年前)
編輯西部地塊最早的地質記錄形成於新太古代,[8]當時發生了大量地殼增生和再造。[10]新太古代岩石主要由綠岩、高級變質岩和花崗岩類構成。[16]礦物檢查顯示了典型的逆時針溫度-壓力-時間路徑,表明新太古代的地殼生長存在侵入和底侵。[17]
固陽花崗綠岩地體
編輯固陽花崗綠岩地體位於西部地塊北部,從色爾騰山向東分佈到東洪生。[10][20][21]這個地體以變質岩和花崗岩為主體。有人認為該岩系可能代表了上層地殼的古老變質作用。[22]
綠岩是前寒武紀變質的超基性岩到鎂鐵質岩石和沉積岩序列。它們在固陽花崗綠岩地體的色爾騰山有完全的出露。[10][20]該岩層的綠岩序列可以劃為3個子單元。低層以變質的鎂鐵質和超基性噴出岩為主,夾有帶狀條狀鐵層。[23]中層由一系列變質火成岩組成,成分從長英質到鎂鐵質不等。頂層主要是變質沉積岩,如石英岩和大理石。[16]據鋯石測年數據,綠岩序列底層形成於約25.4億年前,[24]中層和頂層的年代晚於25.1億年前。[23]
花崗岩類是主要由石英、長石和雲母組成的侵入型火成岩。[25]固陽花崗綠岩帶的花崗岩類主要是TTG岩石和讚岐岩類。[16]TTG岩石的形成有兩個階段,第一階段大約在25.3億年前[26],第二階段在25.2-24.8億年前。[20][27]讚岐岩類形成於TTG岩石形成的兩個階段之間,大約在25.3-25.2億年前。[20][27]
武川高級複合體
編輯武川高級複合體西起朱拉溝,東至西烏蘭布朗。[10]複合體中包括花崗岩類、麻粒岩和紫蘇花崗岩。花崗岩類主要是中(550-650°C)到高級(650-900°C)變質的閃長岩[28],麻粒岩是高級變質的TTG岩石。[10]與固陽花崗綠岩地體相似,武川複合體的岩石的年代也在距今25.5-25億年前左右。[20][29]高級複合體可能是25.5-25億年前變質的下層地殼。[22]
古元古代岩石(25–5.39億年前)
編輯許多研究者提出,華北克拉通西部陸塊是在古元古代(25-16億年前)集合起來的,形成了一個由孔茲岩組成的貫穿西部陸塊的線性結構。[3][1][4][5][7]孔茲岩帶自賀蘭山向東延伸至集寧複合體。[4] Pelitic 麻粒岩、石英岩、長英質副片麻岩和大理石都屬於所謂「孔茲岩系」,沿此帶均有分佈。[10]孔茲岩系是在穩定的大陸坡環境下產生的沉積岩經過變質作用形成的。[4][30][31]通過鋯石測年,可知沉積岩原岩是在23-20億年前沉積的,在19.5-18.7億年前發生變質作用。[8]孔茲岩中的礦物表現出等溫減壓的壓力-溫度路徑,說明沉積原岩可能是在碰撞環境中變質的。[32]
顯生宙地層(5.39億年前至今)
編輯前寒武紀之後,西部地塊變得更加穩定。沉積岩沉寂下來,覆蓋了前寒武紀基岩的一部分。顯生宙也發生了岩漿作用。[2]
寒武紀至奧陶紀早期,西部地塊形成了大量碳酸鹽岩。[33]晚奧陶世到早石炭世幾乎沒有沉積物。[34]晚石炭世和早二疊世期間,碳酸鹽和一些含煤岩石又開始沉積。晚二疊世時,形成了礫岩及紅色含鐵砂岩、粉砂岩和泥岩(紅層)。[35]在三疊紀和侏羅紀,地層以砂岩和泥岩為主。[36][37]砂岩沉積和岩漿作用發生於早白堊世,形成噴出火成岩,如流紋岩、安山岩、玄武岩和英安岩。[38]晚白堊世至新生代的沉積物和新生代玄武岩覆蓋在之前的地層上。[39]
地質階段 | 岩石形成時間 | 岩石 | 位置 |
---|---|---|---|
新太古代 | 2.7 Ga | TTG[8] | 西烏蘭布朗[8] |
2.55–2.50 Ga | 綠片岩、角閃岩、條狀鐵帶、普通角閃石-斜長石片麻岩、副片麻岩、雲母片岩、石英岩、大理石、TTG岩石、石英閃長岩、埃達克岩、讚岐岩類、麻粒岩和紫蘇花崗岩[10][16][23][25][28] | 固陽花崗綠岩地體和武川高級複合體[10] | |
古元古代 | 1.95–1.87 Ga | 泥質麻粒岩、石英岩、長英質副片麻岩和大理石[10] | 孔茲岩帶[10] |
寒武紀 | 539–488 Ma | 碳酸鹽岩[33] | 主要在鄂爾多斯盆地[2] |
奧陶紀 | 488–460 Ma | ||
460–443 Ma | 幾乎沒有[34] | / | |
志留紀 | 443–416 Ma | ||
泥盆紀 | 416–359 Ma | ||
石炭紀 | 359–318 Ma | ||
318–299 Ma | 碳酸鹽岩和含煤岩層[33] | 主要位於鄂爾多斯盆地[2] | |
二疊紀 | 299–270 Ma | ||
270–251 Ma | 紅床和礫岩[35] | ||
三疊紀 | 251–228 Ma | 含沙泥岩、中-高品位砂岩與灰泥岩層[36] | |
228–199 Ma | 高品位砂岩和泥岩,夾煤炭層[36] | ||
侏羅紀 | 199–145 Ma | 中-高品位砂岩、粉砂岩、礫岩、泥板岩和煤炭[37] | |
白堊紀 | 145–65 Ma | 玄武岩、安山岩、英安岩、流紋岩和化石化沉積岩[38] | |
新生代 | 65至今 | 沉積物與玄武岩[2] |
構造劃分
編輯西部地塊的構造劃分仍有激烈爭議。有幾個模型說明了西部地塊的構造劃分,它們給西部地塊的組成部分和結構賦予了不同名稱。這些模型中的西部地塊的面積和形狀相似,但它們間可能並不完全一致。
趙國春等人[1][3][4]提出,華北克拉通西部地塊可以細分為兩個子地塊:陰山地塊和鄂爾多斯地塊。它們間是一個古元古代陸陸碰撞帶,是孔茲岩帶。孔茲岩帶沿東東北-西西南方向橫切整個地塊。
Kusky等人[5][40]則將西部地塊分為3個部分:內蒙古-河北北部造山帶、恆山高原和一個微陸塊。恆山高原南界是一個正斷層,方向為東東北-西西南。東北-西南走向的大同-吳起斷層橫貫西部地塊。
Santosh[41]的想法與趙國春等相似,他將西部地塊分成陰山地塊和鄂爾多斯地塊,但中間的碰撞帶則稱作「內蒙古縫合帶」。不連續的孔茲岩帶暴露在內蒙古縫合帶的南部。
構造演化
編輯前寒武紀歷史
編輯不同地質學家提出了各種西部地塊的演化模式。下面討論三種最流行的解釋前寒武紀基岩構造演化的模型。
趙國春模型
編輯趙國春模型[1][3][4]可以分為兩個主要階段:新太古代地殼增生和古元古代兩個地塊的融合。趙國春等人提出,27億年前,年輕的陰山地塊發生過一次大型地殼增生,形成厚厚的鎂鐵質地殼,儘管還不能確定這一岩漿事件是發生在大陸還是海洋環境中。25.5-25億年前,年輕的陰山地塊被部分熔化,產生大量TTG岩石,覆蓋了整個陰山地塊。約24.5億年前,鄂爾多斯地塊潛沒到陰山地塊下。俯衝板塊的部分熔化形成了花崗岩和噴出岩,如埃達克岩和讚岐岩類。20-19.5億年前,鄂爾多斯地塊北部的沉積岩沉積在穩定的大陸被動邊緣。西部地塊的最終形成發生於約19.5億年前。陰山地塊南部和鄂爾多斯地塊北部相撞時,古海洋關閉。陸陸碰撞的高溫高壓環境產生了兩個地塊間的孔茲岩帶,使得西部地塊其他部分發生變質作用。[1][3][4]
Kusky模型
編輯Kusky模型中,[5][40]古陸塊在35-27億年前形成了年輕的西部陸塊。23億年前,五台弧和一個外來弧分別潛沒到西部地塊的東西兩側。23-20億年前,西部地塊與這兩個弧相撞,東南部形成了恆山花崗岩帶,西北部則形成內蒙古-河北北部造山帶和孔茲岩帶。最終,哥倫比亞超大陸在18億年前的華北克拉通北緣與之發生碰撞。
Santosh模型
編輯不同於趙國春模型和Kusky模型,Santosh[7]提出的西部地塊構造演化主要集中在西部地塊的融合,對碰撞事件發生前的早期構造發展討論較少。Santosh認為,鄂爾多斯地塊是一個由TTG岩石和紫蘇花崗岩組成的大陸弧。在鋯石定年和斷層掃描數據的支持下,Santosh提出陰山地塊和鄂爾多斯地塊在大約19.2億年前發生碰撞,陰山地塊潛沒到鄂爾多斯地塊下。兩個子地塊碰撞後形成了增生楔。玄武岩質洋殼有一部分被納入增生楔。Santosh將增生楔區域命名為內蒙古縫合帶。[7]孔茲岩帶也形成於縫合帶中。[7]
顯生宙歷史
編輯西部地塊在前寒武紀融合後變得穩定。沉積和火山活動開始覆蓋前寒武紀基底。除晚奧陶世至早石炭世的記錄空白外,從寒武紀到侏羅紀,各種類型的沉積岩形成了厚厚的地層。[2]
在早白堊世,由於克拉通破壞,西部地塊的東部出現了廣泛的岩漿活動。當時,華北克拉通的很大一部分被削除,變得不穩定。克拉通破壞主要受太平洋板塊潛沒至亞洲板塊下引發,隨後發生地殼增厚,於是地殼下部無法承受重力,崩解進地幔。[42]這些過程導致了華北克拉通地區的地殼變薄、變形和岩漿活動。雖然大部分岩漿活動發生在東部地塊,但也波及到西部地塊的東部,產生了玄武岩、安山岩、英安岩和流紋岩。在新生代,由於地殼薄,也發生了火山活動並產生玄武岩。[2]
另見
編輯參考
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