華北克拉通東部地塊

編輯連結
維基百科，自由的百科全書
華北克拉通東部陸塊的位置。陰影部分為東部陸塊。由GeoMapApp生成（Ryan等，2009）。[1]

華北克拉通東部陸塊是地球上最古老的大陸之一。它和西部陸塊之間間隔跨華北造山帶，[1]位於中國東北和朝鮮。[1][2]該地塊包含25億年前（截止到 新元古代）的岩石出露。[1]它是研究過去地殼如何形成和相關地質構造環境的理想場所。[1]

地質學家通過研究岩石和地質結構等地質記錄，能推斷出過去的環境和構造事件。東部地塊最古老的組成部分最早形成於40多億年前（冥古宙）。[3]後來在38到18.5億年前（始太古代到古元古代）經歷了許多地質事件，包括反覆發生的火山爆發和變質作用。[1]因此，大多數岩石被重造、於礦物和岩石紋理發生高度變質。由於前新元古代的岩石暴露十分罕見，人們只對27至18.5億年前（新元古代和古元古代）的岩石所誕生的構造環境有所了解。[1]這些環境包括大火成岩省事件、地幔柱活躍、大陸碰撞、裂張和板塊間的隱沒帶。[4][5][6][7][1]膠遼吉帶將兩個較小的板塊（龍崗地塊和狼林地塊）連接在一起，而跨華北造山帶則將東西地塊連接在一起，形成華北克拉通。[1][8]克拉通根部在距今1.3-1.2億年前（白堊紀）被破壞過，岩石圈較薄。[9]

岩石與地質構造[編輯]

冥古宙[編輯]

雖然沒有任何證據表明東部地塊存在冥古宙岩石，但一些冥古宙鋯石的年代經放射性定年法可確定為超過40億年。[10][3]它們分布在鞍山、[10][11][3]河北東部[12][13]和信陽，[14][15]表明這些地區存在冥古宙地殼。

東部地塊中出露的太古宙基岩分布圖和膠遼吉帶的位置。[2]

始太古代[編輯]

始太古代岩石在鞍山十分罕見，覆蓋面積小於20km2。[3]基岩由38–36億年前的奧長花崗岩片麻岩。[10][15][16]它分兩個階段沉積。第一階段發生在約38億年前，第二階段發生在約36億年前。[15][17][16][3][10]這些階段的證據是，較早的片麻岩夾雜在較年輕的奧長花崗岩中，較年輕的奧長花崗岩岩脈橫切過較老的片麻岩岩層。[10]

除深成岩體外，河北東部的變質沉積岩中也發現了大量始太古代鋯石碎屑，鞍山的少些。[3]黑雲母片岩、鉻雲母石英岩和副片麻岩記錄的同位素年齡為38.8–35.5億年前。[18][15]這進一步證明了冥古宙-始太古代地殼的存在，它後來變為變質沉積岩的沉積原岩。[19]

在東部地塊西南緣的信陽，發現了36億年前長英質麻粒岩捕虜岩中的鋯石。[14]這意味着東部地塊西部也可能存在始太古代地殼。[14]

古太古代[編輯]

罕見的古太古代岩石分布在鞍山和河北東部，包含花崗岩類、變質沉積岩和角閃岩。[20][17]35.5億年前，前古元古代沉積岩和花崗岩類發生了變質，[15]變為奧長花崗岩片麻岩和變質沉積岩，包括石英岩、副片麻岩、鈣硅酸鹽岩等。[21]在河北東部的變質沉積岩中發現了小型角閃岩。[22][20]它表明玄武岩的噴發是在35億年前的變質事件之後發生的。[20][22]在鞍山的花崗岩和偉晶岩混合岩中，觀察到奧長花崗岩片麻岩的條紋和透鏡體。[1]它們是受34.5億年前的奧長花崗岩岩漿作用（第三階段）形成的。[15][23][16][1]33.3億年前相似的替換（第四階段）創造了花崗岩類。[17]它還導致了變質沉積岩的形成，包含角閃岩、黑雲母-斜長石片麻岩、石英岩等。[3]

中太古代[編輯]

分散的中太古代岩石一般為火成岩和變質岩，年代為距今32–28億年前。[20][24][25]花崗岩主要分布在鞍山和河北東部。[17][22][21]它們在距今約30億年前安置並結晶。[17][21]同時，變質沉積岩的原岩，包括角閃岩、副片麻岩和石英岩發生沉積。[1]在山東煙臺棲霞市，29-28.5億年前的局部岩漿活動形成了TTG岩石片麻岩的火成母岩。[24][25]此外，除鞍山和河北東部地區外，棲霞市還有中太古代地殼。[24][25]

新太古代[編輯]

除東部地塊東北部稀疏分布的前新太古代岩石外，新太古代岩石構成了出露的地塊基岩的90%。[1]它們主要由TTG岩石片麻岩和少數變質沉積岩組成。有兩組岩石，具有不同的岩性、變質過程和地球化學特徵。[1][26]它們分別形成於距今27.5–26.5和25.5–25億年前。[1][26]較早的一組局部存在於山東，較晚的則遍布整個地塊。[27]

新太古代早期[編輯]

魯西複合體，或稱魯西花崗-綠岩地塊，包含片麻岩和變質的超基性鎂鐵質噴出岩的片狀體和透鏡體（綠岩）。[28][26]變質的科馬提岩反映為蛇紋岩化橄欖岩和帶鬣刺屬紋理的片岩。[1]此種紋理可能與27.4億年前的玄武岩火山活動有關。[27]同樣，棲霞市也發現了27.5–27億年前的棲霞複合片麻岩。[24][29]這兩個地區的岩石意味着在27.5-26.5億年前，花崗岩的早期侵位和火山岩的噴發。[25][24]很快發生了26.5億年前的變質事件，將岩石變為片麻岩和變質沉積岩。[24][25]但兩個地區的片麻岩地質記錄卻略有不同：[24]魯西複合體的片麻岩顯示了26.5、25和19–18.5億年前的變質事件。[25][24]棲霞綜合體的片麻岩則只記錄了較年輕的變質事件。[24]這表明較早的變質事件記錄被後來的覆蓋了。[1]

除此之外，魯西和棲霞的綠岩和片麻岩的形成被認為與27億年前的大火成岩省事件有關。[30][4]岩漿噴出，形成鎂鐵質地殼。[30]

新太古代晚期[編輯]

新太古代晚期岩石遍布整個東部地塊。[1]高、中級片麻岩和超基性噴發岩，特別是科馬提岩出現在河北東部、山東東部、遼寧北部和吉林南部等地，而低、中級花崗岩-綠岩台地則出現在山東西部、遼寧南部和鞍山等地。[31][32][33][28][34][35][36][37]所有岩石都是在25.5-25億年前的一個短暫的地質時期形成的。這一時期，鎂鐵質和長英質岩漿噴出，花崗岩類侵入整個東部地塊，隨後在25億年前發生了區域性的變質作用。[38][24][39][19][40][25][41][31]

變質事件具有逆時針的壓力-溫度-時間路徑，幾乎是等壓冷卻。[42][43][44][45]逆時針路徑表明變質作用與地殼內的岩漿侵入有關。[1]在順時針和峰變質過程中，溫度和壓力劇增，大量鎂鐵質物質增添到地殼中；在峰變質解釋後，岩漿的侵入停止，導致了等壓冷卻。[1]

從結構上看，這些新太古代晚期的岩石大都呈穹丘狀，例如遼寧南部的錦州穹隆和吉林南部的樺甸穹隆、[46][1]這些TTG岩石片麻岩穹丘呈圓形或橢圓形，寬約10–50km。[1]核心區可見紫蘇花崗岩和花崗岩，[1]它們的形成仍有爭議，有人認為它們是由重疊的褶皺形成的，有人則認為它們是由花崗岩岩漿的底闢形成的。[44][1]

古元古代[編輯]

膠遼吉帶[編輯]

東部地塊由兩個子地塊組成，中間被膠遼吉帶連接。[1]膠遼吉帶的西北邊是龍崗地塊（或稱燕遼地塊），東南邊是狼林地塊。[1]

膠遼吉帶內，有花崗岩侵入和變質沉積岩及火山岩序列。[47]花崗岩的侵位發生於22.2億年前，產生了A型花崗岩、鹼性正長岩和環斑花崗岩。[48][49][50][51]它們是一些20-19.5億年前形成的沉積岩和火成岩的原岩。[52][51][50]在吉林南部、山東東部和朝鮮可以發現綠片岩到低級角閃岩相岩石。[53][51][52][54]所有這些岩石都是在19.3–19億年前和18.7億年前變質的。[52][53][51]

由於地層內壓力-溫度-時間路徑的不同，該帶可分為北區和南區。[55]南區的壓力-溫度-時間路徑為逆時針，包括景山、南遼河和吉安組。[56][57]北區的路徑則是順時針，包括粉子山、北遼河和老嶺組。[57][56]

岩石及地質事件總結[編輯]

從地質構造和紋理中，可以推斷出過去的地質事件。東部區塊經歷了多次火山噴發、侵位和變質事件。

時期 十億年前 地質事件 岩石事件 位置
冥古宙

（？-40億年前）

>4 冥古宙地殼形成 冥古宙鋯石 鞍山、河北東部
始太古代

（38–36億年前）

3.8 奧長花崗岩的侵位（第一階段） TTG岩石片麻岩 鞍山
3.6 奧長花崗岩的侵位（第二階段） TTG岩石片麻岩
3.7–3.6 表殼岩的形成 變質沉積岩
古太古代

（36–32億年前）

3.55 變質作用 TTG岩石片麻岩、變質沉積岩 鞍山、河北東部
3.5 玄武岩噴出 曹莊角閃岩 河北東部
3.45 奧長花崗岩的侵位（第三階段） 深溝寺複合體的TTG岩石片麻岩 鞍山
3.33 奧長花崗岩和花崗岩的侵位（第四階段） 東山複合體的TTG岩石片麻岩、陳台溝花崗岩
變質沉積岩的形成 陳台溝變質沉積岩
中太古代

（32–28億年前）

3 花崗岩的侵位 歷山、鐵架山、鞍山和楊亞山花崗岩 鞍山、河北東部
變質沉積岩的形成 遷安變質沉積岩 河北東部
2.9–2.85 奧長花崗岩的侵位 黃崖地TTG片麻岩 棲霞市
新太古代

（28–25億年前）

2.7 大火成岩省事件 魯西綠岩帶科馬提岩、魯西複合體及棲霞複合體的TTG片麻岩 整個東部地塊
2.75–2.65 TTG岩石的侵位、火成岩的噴出 魯西花崗綠岩帶、棲霞複合體的TTG片麻岩 魯西和棲霞
2.65 變質作用 魯西複合體的TTG片麻岩
2.55–2.5 鎂鐵質-長英質岩漿的噴出和TTG岩石的侵位 花崗綠岩帶、TTG片麻岩、紫蘇花崗岩、花崗岩 整個東部地塊
2.5 區域性變質作用 TTG片麻岩、鎂鐵質麻粒岩、角閃岩
古太古代

（22–18.5億年前）

2.2–2 花崗岩的侵位 A型花崗岩、鹼土金屬正長岩、環斑花崗岩 遼寧東部、吉林南部、山東東部和朝鮮
2–1.95 沉積岩-火山岩序列的形成 綠片岩到低級角閃岩相
1.9 膠遼吉帶的形成和變質作用 綠片岩到低級角閃岩相
1.85 華北克拉通東西地塊合併，中間形成跨華北造山帶 片麻岩、上角閃岩到麻粒岩相 跨華北造山帶

構造演變[編輯]

由於前新太古代岩石出露較少，很難斷定當時的構造環境。[1]因此，只能推斷出新太古代以來的構造環境。

新太古代[編輯]

新太古代的兩個岩石群被認為與各種構造環境有關。[1]27億年前左右的岩石與大火成岩省事件有關。[30]然而，學者們對25億年前左右形成的岩石有不同看法。有人提出了岩漿弧模型，還有人提出了地幔柱模型。[58][1]

大火成岩省[編輯]

地幔柱模型顯示了超基性和玄武岩大火成岩省的形成。地球深處的物質上升，侵入岩石圈，拉伸了地殼。大量岩漿在地表噴發，成為大火成岩省。[58]

約27億年前，發生了一次一次大火成岩省事件，具有大規模岩漿作用。它由地幔柱活動引起，使得地殼被拉伸、岩漿侵入，從而使岩石圈熔化。[4][58][30]這樣的模型可以解釋超基性熔岩的噴發和魯西花崗綠岩地塊的科馬提岩及鎂鐵質岩石。[4][30]地幔柱中軸由低黏度超基性物質組成，而地幔柱頂部帶來了較冷的玄武岩物質。[58]因此，岩石具有不同的化學性質。[30][4]

然而，關於大火成岩省仍有許多爭議。大火成岩省可能發生在大陸或海洋環境中。[6][1]此外，大火成岩省事件發生時，東部地塊是否是一個完整、成熟的大陸，仍然是個未知數。[1]

岩漿弧模型[編輯]

岩漿弧系統中，顯示出具有鎂鐵質和長英質物質的岩漿的雙模火山活動。俯衝打樣板塊和下層大陸地殼的部分熔化導致了片麻岩成分的不同。[5]

TTG岩石片麻岩的形成與俯衝過程中岩漿弧的形成有關。[5][59][60]TTG片麻岩的地球化學性質與現代板塊構造下的大陸弧鈣鹼性岩石相近。[5][59][60]在大陸弧系統內，俯衝的大洋板塊和較深的大陸地殼被部分熔化。[5]於是，TTG片麻岩的成分會略有不同，鎂含量可觀察到高低差異。[5]

但有人否定這一模型，因為它只能解釋TTG片麻岩的形成，而不能解釋25億年前岩漿事件的其他特徵。[1]他們提出了下面的地幔柱模型。

地幔柱模型[編輯]

地幔柱模型是針對岩漿弧模型的缺陷提出的。它可以解釋25億年前的岩石的以下特徵，這些特徵不能用岩漿弧模型來解釋：

古元古代[編輯]

19億年前膠遼吉帶的產生一直存在爭議，有人認為它是由弧-陸碰撞產生的，也有人認為它和大陸內部裂谷有關。[50][7]然而，跨華北造山帶一定是在俯衝和大陸碰撞下於18.5億年前形成的。[1]

弧-陸碰撞[編輯]

形成膠遼吉帶的弧-陸碰撞橫截面。[1]

弧-陸碰撞模型中，東部地塊直到古元古代才組合成一個地塊。[66]它是在狼林地塊的火山島弧和元古宙龍崗地塊碰撞之後形成的，形成了膠遼吉帶。[7]遼寧東部的北遼河組超基性到鎂鐵質岩石是在地殼擴張的弧後（弧後盆地）形成的。[7]後來，狼林地塊在龍崗地塊下移動，將南遼河組帶入帶內。[66]遺憾的是，該地區並未發現岩漿弧系統中常見的鈣鹼性岩石。[1]

裂谷閉合模型[編輯]

不同於弧-陸碰撞模型，裂谷閉合模型認為太古宙存在一個連貫的東部地塊。[52][50]它在古元古代早期分裂為龍崗地塊和狼林地塊。中間形成了海洋。[50][52]22-20億年前，隨着地塊開始分離，鎂鐵質和花崗岩熔岩侵入地殼，形成了20-19.5億年前的沉積-火山岩序列。[53][51][67]例如，形成了A型花崗岩、綠片岩和低角閃岩相的鎂鐵質和長英質火成母岩。[68]該帶兩側年齡相近的岩石支持裂谷的觀點。[68]此外，硼酸鹽礦物礦床意味着洋盆的存在。[69]約19億年前，海洋被封閉，兩個地塊發生碰撞。[67][53][21]膠遼吉帶形成，並發生變質作用，這可從泥質麻粒岩中得到證明。[66]

俯衝[編輯]

一系列演化圖顯示了東西地塊的俯衝和陸陸碰撞。形成了跨華北造山帶。[1][70]

除東部地塊東緣的潛沒和碰撞之外，西側邊緣也發生了俯衝。俯衝從25.5億年前持續到18.5億年前。[1]它封閉了東西地塊之間的海洋，形成了跨華北造山帶。[8]

俯衝發生在25.5–24.7億年前。[71]它到孩子了下層地殼和地幔楔的部分熔解。[71]它產生了大量岩漿，形成花崗岩類、綠岩、鎂鐵質和長英質火成岩。[72][73][74][75]隨着俯衝的進行，弧旁區域擴張，形成弧後盆地，岩漿向上流動。23.5-19.2億年前，發生了花崗岩侵入和鎂鐵質岩脈侵入。[1]鎂鐵質岩脈後來變質為鎂鐵質麻粒岩和角閃岩。[1]最終，整個海洋都潛沒到東部地之下。[1]東西地塊大約在18億年前碰撞在一起，[8]並形成中間的跨華北造山帶，形成華北克拉通。[8][76]地塊的碰撞可能和哥倫比亞超大陸的形成有關。[8]

顯生宙[編輯]

華北克拉通此後直到顯生宙（3.24億年前）一直都保持穩定。[9]石炭紀到中三疊世（3.24–2.36億年前），華北克拉通的北緣發生了俯衝。[77][9]於是，古亞洲洋閉合。[9][77]在晚三疊世（2.4-2.1億年前）華北克拉通和揚子克拉通相撞，[9][77]產生秦嶺-大別造山帶。[9][77]在侏羅紀（2-1億年前），古太平洋板塊潛沒到華北克拉通東部之下。[9][77]所有這些俯衝都給下層地殼帶來了像水一樣的流體，[9]使之變得更密、更脆。[9]最終，其下部在白堊紀（1.3–1.2億年前）崩解並沉入地幔。[9][77]接着，上層地殼彈起並被拉開。[9]因此，直到現在，東部地塊的地殼和延伸結構都比較薄，如 渤海灣盆地。[9][77]

另見[編輯]

參考[編輯]

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