沈其韓, 耿元生, 宋會(huì)俠

中國地質(zhì)科學(xué)院地質(zhì)研究所, 北京 100037

華北克拉通的組成及其變質(zhì)演化

沈其韓, 耿元生, 宋會(huì)俠

中國地質(zhì)科學(xué)院地質(zhì)研究所, 北京 100037

華北克拉通早前寒武紀(jì)變質(zhì)基底主要由五套不同類型的變質(zhì)巖系組成?？死ㄔ谛纬蛇^程中經(jīng)歷了多期構(gòu)造活動(dòng)、多期巖漿侵位、多期變質(zhì)作用以及不同程度的混合巖化和深熔作用, 巖石已遭受多次不同地質(zhì)作用的疊加改造, 因此華北克拉通具有復(fù)雜的演化歷史。從太古宙到古元古代末的克拉通形成, 華北克拉通主要經(jīng)歷了五期區(qū)域變質(zhì)作用。鞍山地區(qū)的古—中太古代經(jīng)歷了角閃巖相變質(zhì)作用改造, 尚未獲得變質(zhì)年齡數(shù)據(jù)。但在TTG巖系中已獲得3 560 Ma和3 000～3 300 Ma早期的變質(zhì)年齡。河南魯山太華雜巖的中太古代斜長(zhǎng)角閃巖中獲得2 776～2 792 Ma和2 671～2 651 Ma兩期變質(zhì)作用年齡信息, 代表了新太古代早期的變質(zhì)作用。新太古代麻粒巖-TTG巖系和新太古代花崗-綠巖系都經(jīng)歷了新太古代晚期—古元古代初的變質(zhì)作用改造。在古元古代階段, 在華北克拉通北緣在1 965～1 900 Ma期間發(fā)生了中低壓/高壓麻粒巖相變質(zhì), 局部發(fā)生超高溫變質(zhì), 這期變質(zhì)作用與陸塊間的俯沖碰撞及其后的地幔上涌有關(guān)。在古元古代晚期(1 890～1 800 Ma)在華北克拉通的中部及東部的膠—遼—吉帶發(fā)生了高壓麻粒巖相-角閃巖相的區(qū)域變質(zhì),代表了陸塊間的碰撞拼合過程。不同變質(zhì)巖系類型經(jīng)歷的變質(zhì)作用反映了不同的構(gòu)造背景。太古宙晚期大量的TTG巖系及呈面狀分布的中/低壓麻粒巖主要出露在華北克拉通的中北部, 普遍具有逆時(shí)針的p-T軌跡,反映了地幔柱底板墊托的構(gòu)造環(huán)境。新太古代的花崗-綠巖系在新太古代晚期—古元古代早期經(jīng)歷的變質(zhì)作用多為順時(shí)針的p-T演化軌跡, 反映其發(fā)生可能與弧后+地幔柱聯(lián)合作用的構(gòu)造背景。古元古代晚期的兩期變質(zhì)作用多表現(xiàn)為高壓麻粒巖相的順時(shí)針p-T演化軌跡, 反映了不同陸塊(地塊)之間碰撞拼合的過程, 意味著類似顯生宙的板塊構(gòu)造體制已經(jīng)出現(xiàn)。

華北克拉通; 中低壓/高壓/超高溫變質(zhì)作用; 地幔柱底板墊托; 順時(shí)針/逆時(shí)針p-T軌跡; 碰撞拼合

華北克拉通在1:500萬變質(zhì)地質(zhì)圖上稱為華北變質(zhì)地區(qū), 它是我國最古老和最大的前寒武紀(jì)克拉通之一, 具有早前寒武紀(jì)變質(zhì)結(jié)晶基底和中新元古代沉積蓋層的二元結(jié)構(gòu)格局。

華北克拉通早前寒武紀(jì)的變質(zhì)結(jié)晶基底主要由以下五大部分組成, 它們是: (1)由始太古—古—中太古代TDG巖系為主和少許古—中太古代表殼巖組成的最古老變質(zhì)巖系, 它們僅在鞍山等地局部出露; (2)以新太古代TTG巖系為主伴生新太古代的變質(zhì)表殼巖系的變質(zhì)巖系, 它們多經(jīng)歷了麻粒巖相-角閃巖相的中高級(jí)變質(zhì), 主要在華北克拉通北部分布; (3)新太古代變質(zhì)表殼巖與TTG巖系組成的花崗-綠巖系, 它們一般經(jīng)歷了中低級(jí)變質(zhì)改造, 主要分布在陰山、吉南—遼北、五臺(tái)、魯西、登封等地; (4)已經(jīng)歷高壓-中壓麻粒巖相變質(zhì)的古元古代沉積或火山沉積巖系, 主要分布在華北西北部(孔玆巖帶)及膠東地區(qū); (5)沒有麻粒巖相變質(zhì)的古元古代中深-中淺變質(zhì)的沉積或火山沉積變質(zhì)巖系, 主要分布在滹沱、呂梁、中條、遼河及膠東等地(圖1)。

克拉通在形成過程中經(jīng)歷了多期構(gòu)造變動(dòng), 伴生多期巖漿活動(dòng)和多期變質(zhì)作用以及不同程度混合巖化和深熔作用的影響, 巖石已遭受強(qiáng)烈疊加改造,因此具有復(fù)雜的構(gòu)造-巖漿-變質(zhì)演化歷史。研究華北克拉通的變質(zhì)演化涉及同位素年齡數(shù)據(jù)的應(yīng)用,以往所測(cè)定的Sm-Nd、Rb-Sr和K-Ar年齡數(shù)據(jù)由于測(cè)試精度不高、誤差較大, 因此本文主要以鋯石的原位定年數(shù)據(jù)為依據(jù)。

圖1 華北克拉通變質(zhì)巖系分布簡(jiǎn)圖Fig. 1 Sketch metamorphic map of the North Chian CratonCD-承德; DF-登封; EH-冀東; FP-阜平; GY-固陽; HA-懷安; HL-賀蘭山; HS-恒山; JN-集寧; LL-呂梁; MY-密云; NH-冀北; NL-遼北; QL-千里山; SJ-吉南; TH-太華; WD-烏拉山–大青山; XH-宣化; WL-遼寧西部; WS-魯西; WT-五臺(tái); ZH-贊皇; ZT-中條CD-Chengde; DF-Dengfeng; EH-eastern Hebei; FP-Fuping; GY-Guyang; HA-Huai’an; HL-Helanshan; HS-Hengshan; JN-Jining; LL-Lüliang; MY-Miyun; NH-northern Hebei; NL-northern Liaoning; QL-Qianlishan; SJ-southern Jiling; TH-Taihua; WD-Wulashan–Daqingshan; XH-Xuanhua; WL-western Liaoning; WS-western Shandong; WT-Wutaishan; ZH-Zanhuang; ZT-Zhongtiao

1 華北克拉通始太古代—中太古代的變質(zhì)巖系

始太古—中太古的TDG巖系主要由奧長(zhǎng)花崗質(zhì)片麻巖、石英閃長(zhǎng)質(zhì)片麻巖和花崗巖等組成, 其最大年齡達(dá)3.8 Ga(Liu et al., 1992; Song et al., 1996; Wan et al., 2005; Liu et al., 2008), 變質(zhì)巖系的主體出露于遼寧鞍山一帶, 其中殘留有古太古代變質(zhì)表殼巖, 稱為陳臺(tái)溝表殼巖, 由斜長(zhǎng)角閃巖、黑云變粒巖、黑云斜長(zhǎng)片麻巖、直閃石鐵英巖、直閃石石英巖等組成, 原巖主要是一套玄武質(zhì)和酸性火山巖以及不純硅鐵質(zhì)化學(xué)沉積巖組成, 巖層的主體變質(zhì)已達(dá)角閃巖相, 部分已退變?yōu)榫G片巖相, 原巖時(shí)代為3 300 Ma, 屬古太古代, 但變質(zhì)時(shí)代尚無確切數(shù)據(jù)。這些巖石經(jīng)歷了漫長(zhǎng)的演化歷史, 早期變質(zhì)的變質(zhì)演化史已經(jīng)很難確定, 但在3.77 Ga的條帶狀?yuàn)W長(zhǎng)花崗巖中獲得有3.56 Ga的變質(zhì)年齡, 在一些古太古代片麻巖中獲得有3.0～3.3 Ga的變質(zhì)年齡(Wan et al., 2012a; 董春艷等, 2013)。這些年齡數(shù)據(jù)說明在古太古代期間鞍山地區(qū)的TTG巖系及陳臺(tái)溝表殼巖曾經(jīng)歷過不止一期的變質(zhì)改造, 盡管早期變質(zhì)的礦物組合、變質(zhì)的溫度壓力條件、變質(zhì)作用發(fā)生的構(gòu)造背景已很難追溯, 但是鋯石原位定年的結(jié)果揭示了鞍本地區(qū)古太古代的巖系在古太古代期間曾發(fā)生過變質(zhì)改造。一些作者根據(jù)TTG片麻巖的地球化學(xué)特征, 推斷鞍本地區(qū)3.5～3.6 Ga的TTG片麻巖形成時(shí)的地?zé)崽荻龋?0℃/km(Wan et al., 2005); 有的作者推斷鞍山地區(qū)古太古代的奧長(zhǎng)花崗質(zhì)片麻巖的巖漿源區(qū)的溫度條件為950～1 000℃, 壓力可以達(dá)到1.3～1.4 GPa(Wang et al., 2015)。這樣的地殼地?zé)崽荻群蛶r漿源區(qū)的溫度壓力條件, 說明古太古代期間鞍本地區(qū)已經(jīng)具有相當(dāng)?shù)牡貧ず穸? 具有了發(fā)生區(qū)域變質(zhì)作用的條件。

2 華北克拉通中太古代的變質(zhì)巖系

中太古代中深變質(zhì)表殼巖和TTG變質(zhì)巖系, 以中太古代鐵架山變質(zhì)表殼巖、中太古代遷西曹莊巖組和河南魯山地區(qū)中太古代太華雜巖為代表。

鐵架山變質(zhì)表殼巖呈包體狀產(chǎn)于遼寧鞍山3.0 Ga的鐵架山花崗巖中, 包體規(guī)模很小, 巖石主要是黑云石英片巖、BIF和石英巖等, 已遭受角閃巖相變質(zhì)。包體的形成時(shí)代不會(huì)晚于中太古代, 但變質(zhì)時(shí)代尚不清楚。

分布于河北遷西曹莊—黃白峪地區(qū)的中太古代變表殼巖稱曹莊巖組, 組成巖石包括夕線黑云斜長(zhǎng)片麻巖、斜長(zhǎng)角閃巖、石榴透輝斜長(zhǎng)巖、石榴石英巖、鉻云母石英巖、角閃黑云片巖、條帶狀鐵英巖和鈣硅酸鹽巖等, 原巖相當(dāng)于基性火山巖-沉積建造, 變質(zhì)程度已達(dá)麻粒巖相至高角閃巖相。角閃片麻巖中碎屑鋯石年齡為3 684～3 354 Ma, 強(qiáng)烈重結(jié)晶鋯石的邊部疊加了約2.5 Ga的變質(zhì)年齡(Liu et al., 2013), 它與年齡為3 284～3 129 Ma的英云閃長(zhǎng)質(zhì)片麻巖一起分布于大面積的2.5～2.6 Ga的花崗質(zhì)片麻巖中(Nutman et al., 2011)。畢建成(1989)曾獲得本區(qū)主期麻粒巖相變質(zhì)溫度為750～870℃, 壓力為0.45～0.66 GPa, 屬中溫中壓型變質(zhì)作用, 伍家善等(1998)和閆月華等(1991)曾測(cè)得曹莊組變質(zhì)作用溫壓條件為730～830℃, 0.5～1.0 GPa和溫度＞738℃,壓力＞0.5 GPa, 屬中壓麻粒巖相變質(zhì)作用。在曹莊鐵礦所夾的變基性火山巖(斜長(zhǎng)角閃巖)中獲得了(2859±22) Ma的不一致線上交點(diǎn)年齡(鄭夢(mèng)天等, 2015), 可能代表曹莊巖組的形成時(shí)代, 之后經(jīng)歷了新太古代末—古元古代初的變質(zhì)改造(Nutman et al., 2011; 鄭夢(mèng)天等, 2015)。

分布于河南魯山地區(qū)的太華雜巖(以往稱為下太華巖群), 主要由斜長(zhǎng)角閃巖和TTG巖系組成, 已遭受高角閃巖相變質(zhì)。利用離子探針測(cè)得斜長(zhǎng)角閃巖中鋯石的原巖年齡為2 845～2 838 Ma, 變質(zhì)鋯石年齡第一期為2 776～2 792 Ma, 第二期為2 671～2 651 Ma, TTG的形成年齡為2 832～2 829 Ma, 變質(zhì)年齡為2 772 Ma(Liu et al., 2009), 第五春榮等(2010)應(yīng)用LA-ICP-MS測(cè)得鋯石原巖年齡基本一致。

3 華北克拉通的新太古代變質(zhì)巖系

新太古代變質(zhì)巖系可進(jìn)一步區(qū)分出三個(gè)系列:第一個(gè)系列為麻粒巖-TTG-變質(zhì)巖系, 第二個(gè)系列為新太古代麻粒巖-角閃巖相+TTG變質(zhì)巖系, 第三個(gè)系列為新太古代綠巖花崗巖組合。

3.1 麻粒巖-TTG-變質(zhì)巖系

第一個(gè)變質(zhì)巖系列主要分布于陰山西烏蘭不浪和大青山地區(qū)、遼西建平、遼北清原、冀東、沂水、撫順等地。麻粒巖一般呈東西向面狀分布于大片深變質(zhì)的TTG巖石之中, 變質(zhì)程度達(dá)中低壓高溫麻粒巖相, 有的局部退變?yōu)楦呓情W巖相, 峰期變質(zhì)一般達(dá)800～850℃或更高, 壓力達(dá)0.5～0.9 GPa, p-T軌跡為逆時(shí)針型, 原巖形成時(shí)代為2 560～2 540 Ma,變質(zhì)年齡為2 519～2 480 Ma, 但不同地區(qū)有所差異,如沂水地區(qū)麻粒巖的原巖形成于2 695～2 562 Ma,變質(zhì)作用發(fā)生在2 522～2 509 Ma期間, 2 488 Ma經(jīng)歷了流體改造(趙子然等, 2009)。在麻粒巖中見有變質(zhì)年齡為2 719 Ma的殘余變質(zhì)鋯石(趙子然等, 2009), 表明可能存在新太古代早期的變質(zhì)作用。遼西建平雜巖中麻粒巖形成于2 522～2 520 Ma之間,麻粒巖相變質(zhì)作用發(fā)生于2 490～2 485 Ma(Kr?ner et al., 1998); 原巖為表殼巖的角閃斜長(zhǎng)片麻巖和黑云斜長(zhǎng)片麻巖的結(jié)晶年齡為2 555～2 550 Ma, 閃長(zhǎng)質(zhì)片麻巖的結(jié)晶年齡為(2512±15) Ma, 紫蘇斜長(zhǎng)質(zhì)片麻巖的結(jié)晶年齡為(2510±2) Ma, 它們都經(jīng)歷了新太古代末—古元古代初(2 512～2 471 Ma)的變質(zhì)改造(Liu et al., 2011)。這一系列變質(zhì)巖的麻粒巖相p-T軌跡均為逆時(shí)針型, 其代表性的p-T軌跡如圖2所示。這一系列大量的TTG片麻巖和逆時(shí)針的中低壓麻粒巖相變質(zhì)特點(diǎn)表明其形成與大規(guī)模的地幔上涌有關(guān), 標(biāo)志著克拉通的形成。

圖2 華北克拉通基底太古宙麻粒巖的代表性p-T軌跡Fig. 2 The p-T paths of Archean granulite in North China Craton basementa-1-大青山—烏拉山地區(qū), 引自Zhao et al., 1999; a-2-固陽—武川地區(qū), 引自Zhao et al., 1999; b-冀東—遼西地區(qū), 引自盧良兆等, 1998; c-山東沂水地區(qū), 引自蘇尚國等, 1997; d-吉南—遼北地區(qū), 1和2引自孫德育等, 1993, 3引自葛文春等, 1994a-1-Daqingshan–Wulashan region, after Zhao et al., 1999; a-2-Guyang–Wuchuan region, after Zhao et al., 1999; b-eastern Hebei–western Liaoning region, after LU et al., 1998; c-Yishui region, Shandong Province, after SU et al., 1997; d-southern Jilin–northern Liaoning region, 1 and 2 after SUN et al., 1993, 3 after GE et al., 1994

3.2 麻粒巖-角閃巖相+TTG變質(zhì)巖系

新太古代第二個(gè)系列為角閃巖相為主夾麻粒巖相變質(zhì)表殼巖和TTG巖系, 主要見于太行山阜平和贊皇等地區(qū)。阜平地區(qū)的阜平雜巖原巖為火山-沉積巖系, 變質(zhì)程度達(dá)高角閃巖相至麻粒巖相, Zhao等(1999)和劉樹文(1996)分別對(duì)巖系中的基性麻粒巖做過峰前、峰期、峰期后的礦物共生組合和溫度條件的研究, 均得出一條順時(shí)針軌跡(圖3c, e)。據(jù)劉樹文(1996)研究, 其峰期階段的礦物共生組合為Grt+Cpx+Pl+Hy, 形成溫度為670～740℃, 壓力為0.55～0.7 Ga。TTG巖系的形成年齡最大的達(dá)(2708±8) Ma, 大部分在2 513～2 543 Ma之間, 變質(zhì)年齡在1 875～1 717 Ma之間。新太古代贊皇群主要由(石榴子石)黑云斜長(zhǎng)片麻巖、石榴藍(lán)晶黑云斜長(zhǎng)片麻巖、斜長(zhǎng)角閃巖等組成, 其中斜長(zhǎng)角閃片巖具有三階段的變質(zhì)演化, 組成一條順時(shí)針軌跡(肖玲玲等, 2011; 圖3f)。

3.3 花崗-綠巖組合中的綠巖變質(zhì)巖系

新太古代第三個(gè)系列變質(zhì)巖系為花崗巖-綠巖組合, 又可分為兩個(gè)亞大類。第一亞類綠巖為由綠片巖相至角閃巖相的沉積和火山沉積+BIF組成的變質(zhì)巖系; 第二亞類的變質(zhì)巖系由麻粒巖相至高角閃巖相的沉積和火山沉積+BIF組成的深變質(zhì)巖系。

第一亞類綠巖主要分布于吉南板石溝、遼北清原、遼寧鞍本、魯西、河北灤縣—青龍、山西五臺(tái)、內(nèi)蒙固陽色爾騰山、河南登封等地; 另一亞類由深變質(zhì)的麻粒巖相至角閃巖相的沉積和火山沉積巖加BIF的變質(zhì)巖系, 以往許多學(xué)者將其歸入中太古代,但最近的測(cè)年結(jié)果都屬新太古代, 它們主要分布于河北遷安—遷西和遵化以及北京密云等地。

圖3 新太古代五臺(tái)群(a, b)、阜平群(c, e)、色爾騰山群(d)和贊皇群(f)中基性麻粒巖、斜長(zhǎng)角閃巖和泥質(zhì)片麻巖的p-T軌跡Fig. 3 The p-T paths of amphibolite and pelitic gneiss in Wutai Group (a and b), basic granulite and pelitic gneiss in Fuping Group (c and e), amphibolite in Sertengshan Group (d) and Zanhuang Group (f)

現(xiàn)以山西五臺(tái)、內(nèi)蒙古色爾騰山、魯西、遼寧鞍本、遼北清原、河南登封幾個(gè)地區(qū)為例介紹其變質(zhì)演化特征。

山西五臺(tái)綠巖由下而上分為繁峙亞群、石嘴亞群和臺(tái)懷(高凡)亞群, 屬變質(zhì)的火山沉積巖系, 總體變質(zhì)程度達(dá)綠片巖相-角閃巖相, 下部繁峙群以鐵鋁榴石帶和十字石+藍(lán)晶石帶為主, 缺少綠泥石帶, 中上部主要為綠泥石帶, 五臺(tái)山北坡石榴云母片巖經(jīng)歷了4個(gè)階段的變質(zhì)演化, 早期階段為進(jìn)變質(zhì)階段, 為低壓相系, 峰期階段T=630℃, p= 0.9 GPa, 峰后階段溫度略有升高, 壓力下降T= 660℃, p=0.75 GPa。退變階段為降溫降壓, 整體構(gòu)成一條順時(shí)針軌跡。原巖形成年齡為2 530～2 520 Ma,認(rèn)識(shí)比較一致。變質(zhì)年齡則爭(zhēng)論較大, Liu等(1985)認(rèn)為石咀亞群黑云變粒巖(2508±2) Ma的單顆粒鋯石U-Pb年齡代表了五臺(tái)群的區(qū)域變質(zhì)時(shí)代; Zhao等(2000)認(rèn)為五臺(tái)地區(qū)不存在新太古代的變質(zhì)事件; Liu等(2006)根據(jù)金崗庫組藍(lán)晶石石榴石片巖中獨(dú)居石的測(cè)年結(jié)果認(rèn)為1 887～1 822 Ma是五臺(tái)群的變質(zhì)作用時(shí)代; Qian等(2013)認(rèn)為五臺(tái)群變質(zhì)年齡為1.95 Ga; 楊崇輝等(2015)根據(jù)五臺(tái)群上覆的滹沱群底部礫巖中含有與五臺(tái)群片巖和BIF礫石等地質(zhì)特征認(rèn)為五臺(tái)群的變質(zhì)應(yīng)在滹沱群沉積之前, 很可能在新太古代末期。

內(nèi)蒙古固陽色爾騰山花崗綠巖帶由超過1 000 km2的低級(jí)變質(zhì)的TTG巖系和部分綠巖層序所組成, 綠巖巖層包括超鎂鐵質(zhì)(科馬提巖質(zhì))、基性-長(zhǎng)英質(zhì)堿性火山巖, 底部基性巖中含有BIF, 巖石已變質(zhì)為綠片巖相至低角閃巖相, 原巖形成于裂谷環(huán)境, 綠片巖相的溫度下限為400℃左右(李樹勛等, 1994), 綠巖帶底部石榴斜長(zhǎng)角閃巖已變質(zhì)為角閃巖相, 據(jù)李樹勛等(1987)和金巍(1989)的研究(轉(zhuǎn)引自Zhao et al., 1999)其變質(zhì)過程為: M1變質(zhì)階段的礦物共生組合為Chl+Ep+富鈉Pl, 多為包裹體包于石榴子石顆粒中, 是基性巖的典型綠片巖相礦物組合, 形成溫度為400℃, 壓力平均為0.25 GPa; M2階段為峰期階段, 礦物共生組合為Hbl(核)+Pl(核An30)+Qtz±Grt, 形成溫度為635℃, 壓力為0.5 GPa; M3階段為退變質(zhì)階段, 礦物共生組合為Act+Ep+Pl(邊An26)+Qtz, 形成溫度為450℃, 壓力為0.5 GPa, 顯示近等壓冷卻, 總體為一條逆時(shí)針p-T軌跡(圖3d), 但有爭(zhēng)論。色爾騰山綠巖的原巖時(shí)代為2 560～2 570 Ma(劉利等, 2012), 奧長(zhǎng)花崗巖的年齡為(2 520±9) Ma, 埃達(dá)克質(zhì)閃長(zhǎng)巖的年齡為(2 559±14) Ma(簡(jiǎn)平等, 2005), 英云閃長(zhǎng)巖的年齡為(2 516±7) Ma, 變質(zhì)年齡大體在2 489～2 455 Ma之間。

魯西花崗巖-綠巖帶中的綠巖主要由新太古代的泰山巖群和濟(jì)寧巖群組成, 泰山巖群呈北北西向帶狀分布于泰山西南峪、新泰雁翎關(guān)、柳橋等地; 濟(jì)寧巖群分布于北東向滋陽山一帶, 被覆蓋于蓋層之下, 地表未見出露。泰山巖群主要由斜長(zhǎng)角閃巖、黑云變粒巖、透閃陽起片巖、變質(zhì)礫巖、石榴黑云石英巖及超鎂鐵質(zhì)科馬提巖等組成, 原巖為一套超鎂鐵質(zhì)和基性火山巖夾科馬提巖, 有變余枕狀構(gòu)造,杏仁構(gòu)造和鬣刺結(jié)構(gòu), 變質(zhì)作用達(dá)角閃巖相。泰山巖群可分為晚太古代早期的孟家莊巖組、雁翎關(guān)巖組和柳杭組下部, 巖石形成年齡為2 750～2 700 Ma,變質(zhì)年齡為2 690～2 640 Ma(杜利林等, 2003, 2005;陸松年等, 2008), 這期變質(zhì)作用是魯西地區(qū)重要的構(gòu)造熱事件(萬渝生等, 2012)。太古代晚期的山草峪組、柳杭組上部, 巖群中富含BIF, 其變質(zhì)程度已達(dá)角閃巖相, 原巖形成年齡2 540～2 530 Ma, 區(qū)域變質(zhì)作用和深熔年齡為2 500 Ma(Wang et al., 2014)。濟(jì)寧巖群亦含BIF, 變質(zhì)程度為綠片巖相, 形成年齡為2 561～2 520 Ma, 變質(zhì)年齡為2 500～2 490 Ma (王偉等, 2010; Wan et al., 2012b)。據(jù)山東省區(qū)域地質(zhì)志(2013送審稿)報(bào)道, 泰山群雁翎關(guān)組斜長(zhǎng)角閃巖的變質(zhì)演化可分為3個(gè)階段: 峰期變質(zhì)階段, 變質(zhì)程度達(dá)高角閃巖相, 礦物共生組合為Hbl1+Pl+Qtz+Bt, 形成的溫度為532～600℃, 壓力為0.6 GPa, 峰后近等壓降溫, 礦物共生組合為Hbl2+Pl±Qtz±Bt, Act+Bt+Pl±Qtz, 變質(zhì)溫度為443～550℃, 壓力為0.4～0.5 GPa, 后期韌性剪切疊加, 變質(zhì)達(dá)綠片巖相, 礦物共生組合為Chl+Ab+Qtz, Act+Ab+Chl+Qtz, Ep+Chl+Ab, 溫度為450℃, 壓力為0.15 GPa。

遼寧鞍山—本溪花崗-綠巖帶的綠巖, 主要指狹義的鞍山群, 暫未包括其下部的深變質(zhì)巖系, 巖石包括黑云變粒巖、斜長(zhǎng)角閃巖、條帶狀鐵英巖、陽起鐵英巖夾少量各種片巖(例如石榴石英黑云片巖、絹云綠泥石英片巖、二云石英片巖等), 是一套以英安質(zhì)火山凝灰?guī)r、基性火山巖、泥質(zhì)-粉砂質(zhì)沉積巖以及硅鐵質(zhì)化學(xué)沉積巖等組成的火山-沉積建造, Zhai等(1990)對(duì)綠巖帶中的斜長(zhǎng)角閃巖、條帶狀鐵礦的地球化學(xué)、變質(zhì)作用和巖石成因做過較詳細(xì)研究。巖石已變質(zhì)為綠片巖相至低角閃巖相, 局部達(dá)高角閃巖相, 不同的地區(qū)變質(zhì)相有些差別, 如在鞍山地區(qū)的東西鞍山、大孤山、齊大山至眼前山一帶, 巖石的變質(zhì)程度達(dá)綠片巖相, 遼陽弓長(zhǎng)嶺、本溪歪頭山、南芬等地的巖石變質(zhì)程度一般達(dá)低角閃巖相, 局部達(dá)高角閃巖相, 變質(zhì)溫度一般為550～650℃, 壓力為0.3～0.6 GPa, 相當(dāng)于低-中壓,變質(zhì)巖系的原巖形成時(shí)代為2 540～2 530 Ma, 變質(zhì)時(shí)代為2 481～2 409 Ma(Cui et al., 2013; 代堰锫等, 2013)。

冀東地區(qū)的花崗巖-綠巖帶分布于灤縣、灤南、盧龍、青龍一帶, 綠巖主要以灤縣群和朱杖子群/雙山子群為代表, 以富含BIF為特征, 灤縣群的變質(zhì)巖主要包括黑云變粒巖(為主), 斜長(zhǎng)角閃巖、黑云長(zhǎng)石石英巖、條帶狀鐵英巖、鎂鐵閃石或鐵閃石石英巖、陽起石英巖和次透閃石巖, 原巖為一套中酸性凝灰?guī)r、凝灰質(zhì)黏土半黏土巖及粉砂巖和化學(xué)沉積的鐵硅質(zhì)建造, 變質(zhì)相以低角閃巖相為主, 局部出現(xiàn)高角閃巖相或高綠片巖相, 原巖的形成年齡為(2 543±8) Ma(Nutman, 2011), 其變質(zhì)年齡為2 500 Ma左右。朱杖子/雙山子群的變質(zhì)巖主要為絹云母石英片巖、黑云母類片巖、石榴云母石英片巖夾角閃石英片巖、條帶狀鐵英巖, 原巖為一套陸源的黏土半黏土質(zhì)和粉砂質(zhì)沉積巖, 夾少量中基性火山巖和中基性凝灰?guī)r, 變質(zhì)程度為低角閃巖相-高綠片巖相,原巖的形成年齡朱杖子群為(2 511±12) Ma, 雙山子群為(2 503±13) Ma, 扎欄杖子BIF夾層黑云斜長(zhǎng)變粒巖的形成年齡為(2 572±8) Ma。變質(zhì)作用時(shí)間約為2 500 Ma, 可能與華北克拉通東部陸塊發(fā)生的巖漿底侵作用有關(guān)(陳靖等, 2015)。

遼北清原新太古代花崗-綠巖帶出露面積約8 000 km2, 70％為花崗質(zhì)巖石, 綠巖僅占30％(Zhai et al., 1985)。綠巖帶由下而上可分為三個(gè)巖組: 下部石棚子巖組主要由斜長(zhǎng)角閃巖、輝石角閃巖, 少量層狀黑云斜長(zhǎng)片麻巖、淺色含黑云母片麻巖組成,下部原巖為超基性-基性火山巖夾數(shù)層科馬提巖, 中部原巖為一系列海相拉斑玄武巖夾薄層和透鏡狀科馬提巖, 上部原巖為雙峰式火山巖。變質(zhì)程度達(dá)角閃巖相, 局部麻粒巖相。中部紅透山組主要有互層狀薄層斜長(zhǎng)角閃巖、黑云斜長(zhǎng)片麻巖和含夕線石、藍(lán)晶石的石英片麻巖組成, 夾塊狀硫化物銅礦。其原巖為鈣堿性火山巖, 底部為拉斑玄武巖-安山巖-流紋巖, 上部夾有拉斑玄武巖、安山巖、英安巖和少量泥質(zhì)巖, 含銅礦。上部南天門組主要由黑云斜長(zhǎng)片麻巖、白云-黑云石英片巖、細(xì)粒角閃斜長(zhǎng)片麻巖、磁鐵石英巖、大理巖和石英巖等組成。巖石變質(zhì)程度近于角閃巖相。整個(gè)綠巖帶變形強(qiáng)烈, 構(gòu)造復(fù)雜, 原巖時(shí)代相當(dāng)于新太古代, 尚缺少變質(zhì)年齡數(shù)據(jù)。

河南登封地區(qū)的花崗巖-綠巖帶中綠巖主要以登封群為代表, 呈不規(guī)則體分布于花崗質(zhì)片麻巖中,它由斜長(zhǎng)角閃巖、角閃變粒巖、黑云變粒巖及各種片巖, 局部有少量鐵英巖組成, 是一套泥質(zhì)中酸性-基性火山-沉積建造, 變質(zhì)程度高峰期達(dá)中壓角閃巖相, 部分為綠片巖相, 游振東和韓玉菁(1981)曾測(cè)定斜長(zhǎng)角閃巖變質(zhì)溫度為550～600℃, 壓力為0.45 ～–0.75 GPa, 變質(zhì)巖的形成時(shí)代為2 530～2 520 Ma,變質(zhì)時(shí)代可能為2 508 Ma(萬渝生等, 2009)。

第一亞類花崗-綠巖系中變質(zhì)綠巖的p-T軌跡多為順時(shí)針軌跡, 個(gè)別為逆時(shí)針軌跡(圖2)。至于這類花崗-綠巖帶的形成構(gòu)造環(huán)境一直存在爭(zhēng)議, 主要有兩種觀點(diǎn): 島弧巖漿作用和地幔柱作用。

第二亞類為深變質(zhì)的新太古期的變質(zhì)巖系, 主要分布于河北遷安、遷西遵化和北京的密云等地區(qū),有的學(xué)者將其歸入深變質(zhì)綠巖系列, 變質(zhì)巖石主要包括中-基性麻粒巖、斜長(zhǎng)角閃巖、輝石巖、鐵英巖、黑云斜長(zhǎng)片麻巖等, 分布于TTG 巖系和花崗質(zhì)片麻巖中, 北京密云、河北遷西、遷安等地的變質(zhì)巖已變質(zhì)達(dá)中低壓麻粒巖相, 局部出現(xiàn)退變的高角閃巖相, 遵化地區(qū)的遵化群變質(zhì)程度已達(dá)高角閃巖相,部分達(dá)麻粒巖相。遷安水廠與BIF呈互層的斜長(zhǎng)角閃巖的形成年齡為(2 547±7)Ma, 變質(zhì)年齡為(2 513±4) Ma(Zhang et al., 2011), 遵化石人溝的同類巖石原巖的形成年齡為(2 553±41)～(2 541±21) Ma, 變質(zhì)年齡為(2 512±13)～(2 516±21) Ma (Zhang et al., 2012)。密云地區(qū)密云群的形成年齡為2 540 Ma, 變質(zhì)年齡為2 449 Ma(Shi et al., 2012)。總體上, 三地變質(zhì)巖石原巖形成年齡為2 540 Ma左右,變質(zhì)作用年齡為2 512～2 490 Ma。

以上兩個(gè)亞類的新太古代花崗-綠巖系中變質(zhì)巖系在原巖建造、形成時(shí)代和變質(zhì)所用時(shí)間等方面都非常相近, 可能屬同一大地構(gòu)造環(huán)境下的產(chǎn)物,只是所處的深度不同而已。

4 古元古代的高壓麻粒巖和TTG組合

古元古代高壓麻粒巖相變質(zhì)的火山-沉積巖系和TTG組合, 高壓麻粒巖大致沿兩條構(gòu)造帶出現(xiàn)(李江海等, 1998), 北亞帶高壓麻粒巖主要見于西部孔茲巖帶東段集寧地區(qū)東南側(cè)的TTG雜巖基底中,大致沿赤城沃麻坑、宣化二道嶺、水地莊、西葛峪、西望山、萬全柳溝, 尚義地上、大虎溝、天鎮(zhèn)四方墩、興和黃土窯等地分布。在赤城沃麻坑地區(qū)除見有高壓基性麻粒巖, 尚見有高壓泥質(zhì)麻粒巖(馬軍等, 1995), 圍巖以TTG片麻巖為主。南亞帶高壓麻粒巖出現(xiàn)于恒山—五臺(tái)山綠巖帶北側(cè)的片麻巖基底中, 從懷安蔓菁溝經(jīng)渾源東部到恒山長(zhǎng)城溝、黃土坡、張崖、山岔、天京等地, 圍巖以花崗片麻巖為主, 在恒山白馬石北部還發(fā)現(xiàn)退變榴輝巖(翟明國等, 1995), 除高壓泥質(zhì)麻粒巖呈薄層狀?yuàn)A于高壓基性麻粒巖中外, 高壓基性麻粒巖成透鏡狀、布丁狀、或似層狀、巖墻狀分布于TTG巖系或花崗質(zhì)片麻巖之中, 基性麻粒巖大部分為巖漿成因。許多高壓基性麻粒巖保存了Grt(高Ca核部)+Pl+Cpx+Qtz的高壓麻粒巖相礦物組合(M1), Grt+Pl+Cpx+Opx+Qtz的中壓麻粒巖相礦物組合(M2), Opx+Cpx+Pl+Qtz的低壓麻粒巖相組合(M3)和Hbl+Pl的角閃巖相礦物組合。另外, 在恒山和蔓菁溝產(chǎn)出的高壓麻粒巖保存了早期榴輝巖相的Grt+Qtz+Omp(假象)的礦物組合。高壓基性麻粒巖的峰期溫度一般在780～850℃,壓力達(dá)1.3～1.5 GPa。變質(zhì)過程組成的p-T軌跡顯示為順時(shí)針軌跡, 峰期起顯示近等溫降壓, 之后為降溫降壓, 圖4為這些軌跡的代表。

高壓泥質(zhì)麻粒巖典型的礦物組合為藍(lán)晶石+三元長(zhǎng)石和藍(lán)晶石+石榴石+金紅石(馬軍等, 1995)。

高壓麻粒巖的形成時(shí)代過去一直認(rèn)為是新太古代, 近來更多的學(xué)者趨向于它們形成于古元古代(約1 915 Ma左右), 變質(zhì)時(shí)代在1 850 Ma左右。也有的學(xué)者認(rèn)為高壓基性麻粒巖形成和變質(zhì)的時(shí)代更老, 1 850 Ma經(jīng)歷的是大面積的高角閃巖相變質(zhì)事件(初航等, 2012)。多數(shù)學(xué)者認(rèn)為高壓基性麻粒巖形成于俯沖碰撞的大地構(gòu)造環(huán)境。

圖4 恒山—懷安壓麻粒巖帶代表性變質(zhì)演化p-T軌跡(a-懷安地區(qū), 據(jù)Guo et al., 2012; b-恒山地區(qū), 據(jù)O’Brien et al., 2005; c-懷安地區(qū)基性麻粒巖, 轉(zhuǎn)引自Zhao, 2000; d-懷安地區(qū)富鋁片麻巖, 據(jù)劉福來, 1995)Fig. 4 The p-T paths of high-pressure granulites of basic granulite in Huai’an area (a, after Guo et al., 2012), of basic granulite in Hengshan area (b, after O’Brien et al., 2005), of basic granulite in Huai’an area (c, after Zhao, 2000); and of rich-Al gneiss in Huai’an area (d, after LIU, 1995)

第二種類型是含有中低壓/高壓麻粒巖、超高溫麻粒巖或只含高壓麻粒巖的古元古代變質(zhì)孔茲巖系。前者主要分布于華北克拉通北部孔玆巖帶的賀蘭山—千里山、烏拉山—大青山和集寧及其相鄰地區(qū), 后者主要見于膠北萊西—平度一帶的荊山巖群分布區(qū)和河南嵩山的孔茲巖系中。

華北北緣變質(zhì)孔茲巖系在西段的賀蘭山—千里山地區(qū)見有中低壓麻粒巖(Zhao et al., 1999)和高壓泥質(zhì)麻粒巖(周喜文和耿元生, 2009; Yin, 2010;周喜文等, 2010; Yin et al., 2011), 在中-東段的大青山和集寧及其相鄰地區(qū)見有高壓基性麻粒巖, 而在大青山東坡和集寧的土貴烏拉和和林格爾地區(qū)見有具假藍(lán)寶石+石英組合和尖晶石+石英組合, 變質(zhì)溫度達(dá)到950～1 000℃的超高溫泥質(zhì)麻粒巖(Santosh et al., 2006, 2007a, 2007b, 2009a, 2009b, 2012, 2013; Santosh and Kusky, 2010; Tsunogae et al., 2011; Liu et al., 2012; Guo et al., 2012)?，F(xiàn)有的同位素年代學(xué)數(shù)據(jù)顯示, 華北北緣孔玆巖帶在1 950 Ma前后經(jīng)歷了高壓/中低壓的麻粒巖相變質(zhì), 在1 920 Ma左右大青山東坡和集寧地區(qū)孔茲巖系中富鋁的泥質(zhì)巖石遭受到超高溫麻粒巖相改造。1 920 Ma的年齡向西可以延伸到千里山地區(qū), 但是該地區(qū)未發(fā)現(xiàn)超高溫的泥質(zhì)麻粒巖。

中低壓/高壓麻粒巖的變質(zhì)演化軌跡均顯示出等溫降壓的順時(shí)針軌跡, 超高溫泥質(zhì)麻粒巖則顯示出逆時(shí)針的變質(zhì)演化軌跡(圖5), 它們是在不同變質(zhì)條件下連續(xù)發(fā)展過程中形成的。趙國春提出, 華北克拉通北緣孔玆巖帶是由陰山陸塊與鄂爾多斯陸塊在1 950 Ma左右相互碰撞、地殼加厚, 導(dǎo)致了高壓麻粒巖相變質(zhì)作用; 在地殼回返過程中, 1 920 Ma左右地幔上涌帶來的熱源導(dǎo)致超高溫麻粒巖相的變質(zhì)。但最近的研究資料顯示, 鄂爾多斯盆地深部出露的巖石與賀蘭山—千里山出露的古元古代孔茲巖系基本一致(Wan et al., 2013), 它們總體呈面狀分布。只是賀蘭山—千里山的巖石出露地表, 而鄂爾多斯地區(qū)的孔茲巖系被深埋地下, 其上被寒武—奧陶紀(jì)和中生代地層所覆蓋。陰山陸塊與鄂爾多斯陸塊碰撞之說成了疑問, 需要進(jìn)一步深入研究。

圖5 華北克拉通西部孔玆巖帶高級(jí)變質(zhì)巖的p-T軌跡Fig. 5 The p-T paths of high-grade metamorphic rocks of western khondalite belt, North China Cratona-賀蘭山—千里山地區(qū); b-大青山烏拉山地區(qū); c-集寧和大青山東坡超高溫麻粒巖; d-集寧—大同地區(qū)(1-集寧孔茲巖系(Zhao et al., 1999); 2-集寧基性麻粒巖(Zhao et al., 1999); 3-集寧孔茲巖系第一次變質(zhì)事件的p-T軌跡(盧良兆等, 1992); 4-集寧孔茲巖系第二次變質(zhì)事件的p-T軌跡(盧良兆等, 1992); 5-大同以東孔茲巖系的p-T軌跡(劉福來, 1997); 6-集寧孔茲巖中高壓泥質(zhì)麻粒巖(Wang et al., 2011); 7-大同孤山高壓石榴基性麻粒巖的p-T軌跡(王洛娟等, 2011); 8-集寧孔茲巖系中石榴石巖的p-T軌跡(Jiao et al., 2013); 9-集寧三岔口孔茲巖的p-T軌跡(蔡佳等, 2014))a-Helanshan–Qianlishan region; b-Daqingshan–Wulashan region; c-eastern slope of Jining and Daqingshan: HT granulites; d-Jining–Datong region(1-Jining khondalite(Zhao et al., 1999), 2-Jining basic granulite(Zhao et al., 1999); 3-p-T path of first metamorphic epoch(LU et al., 1992); 4-p-T of second metamorphic epoch(LU et al., 1992); 5-p-T path of khondalite in eastern Datong(LIU, 1997); 6-HP pelitic granulite in Jining khondalite(Wang et al., 2011); 7-p-T of HP garnet basic granulite in Gushan, Datong(WANG et al., 2011); 8-p-T path of granulite in Jining khondalite(Jiao et al., 2013); 9-p-T path of khondalite in Sanchakou, Jining(CAI et al., 2014))

膠北萊西—平度一帶的荊山群屬古元古代變質(zhì)巖系, 與其北側(cè)出露的粉子山群為同時(shí)異相沉積,但粉子山群不含高壓泥質(zhì)麻粒巖, 變質(zhì)作用僅達(dá)角閃巖相, 趙國春(未刊資料)曾認(rèn)為其變質(zhì)p-T軌跡為順時(shí)針型。荊山群變質(zhì)巖系主要是一套變泥砂質(zhì)沉積巖系, 變質(zhì)程度為角閃巖相-麻粒巖相, 高壓基性麻粒巖和泥質(zhì)麻粒巖呈透鏡狀產(chǎn)出。最初, 盧良兆等(1996)曾測(cè)得其變質(zhì)巖具有逆時(shí)針的變質(zhì)演化軌跡。周喜文等(2004)首次在荊山群中發(fā)現(xiàn)高壓泥質(zhì)麻粒巖, 并具有順時(shí)針p-T軌跡。Tam等(2012a, b)也對(duì)荊山群的高壓泥質(zhì)麻粒巖進(jìn)行了研究, 認(rèn)為其具有順時(shí)針的p-T演化軌跡, 但與周喜文等(2004)所確定的p-T演化軌跡形態(tài)有較大差異(圖6)。同位素年齡資料表明, 荊山群的變質(zhì)作用發(fā)生在1 901～1 838 Ma期間, 屬于古元古代末期(劉平華等, 2011)。早期的研究認(rèn)為荊山群的形成與變質(zhì)發(fā)生在裂谷環(huán)境, 后來的研究多認(rèn)為其形成與碰撞環(huán)境有關(guān)(Zhao and Zhai, 2013)。

圖6 膠北地體中高壓基性麻粒巖、高壓泥質(zhì)麻粒巖的變質(zhì)演化p-T軌跡Fig. 6 The metamorphic p-T paths of M-HP basic granulites and HP pepitic granulites in Jiaobei terraina-膠北地體中高壓泥質(zhì)麻粒巖(Tam et al., 2012a); b-膠北地區(qū)TTG片麻巖中高壓基性麻粒巖(劉平華等, 2010); c-膠北地體中荊山群高壓泥質(zhì)麻粒巖(周喜文等, 2004); d-荊山群中壓泥質(zhì)麻粒巖(Tam et al., 2012b)a-M-HP pelitic granulite(Tam et al., 2012a); b-M-HP basic granulite in TTG gneiss(LIU et al., 2010); c-HP pelitic granulite of Jingshan Group(ZHOU et al., 2004); d-pelitic granulite of Jingshan Group(Tam et al., 2012b)

圖7 河南洛寧地區(qū)古元古代魯山群斜長(zhǎng)角閃巖(a)和泥質(zhì)片麻巖(b)變質(zhì)演化p-T軌跡(據(jù)蔣宗勝等, 2011)Fig. 7 The p-T paths of amphibolite (a) and pelitic gneiss (b) from Paleoproterozoic Lushan Group complex, Henan Province (after JIANG et al., 2011)

河南魯山一帶的古元古代魯山巖群(原稱為上太華群)是含麻粒巖的變質(zhì)巖系。巖石主要包括石墨石榴夕線片麻巖、二云母石英片巖、斜長(zhǎng)角閃巖、大理巖、石榴斜長(zhǎng)角閃巖等, 并夾有石榴二輝麻粒巖(孫勇, 1983)。在河南洛寧地區(qū)的同時(shí)代巖系, 不論是石榴斜長(zhǎng)角閃巖還是泥質(zhì)麻粒巖都記錄了順時(shí)針的近等溫降壓型p-T軌跡(蔣宗勝等, 2011; 詳見圖7)。斜長(zhǎng)角閃巖峰期變質(zhì)年齡在1 938～1 967 Ma間(蔣宗勝等, 2011), 石墨石榴夕線片麻巖的變質(zhì)鋯石年齡為(1 844±66) Ma, 片麻狀石榴花崗巖中變質(zhì)鋯石年齡為(1 871±14) Ma(Wan et al., 2006)。不同巖石測(cè)定的變質(zhì)年齡結(jié)果有一些差別, 但基本可以確定其變質(zhì)時(shí)代為古元古代晚期, 比中央造山帶的碰撞年齡1 850 Ma更早一些。

5 不含高壓麻粒巖的古元古代變質(zhì)巖系

主要分布于阜平—贊皇、五臺(tái)滹沱、中條呂梁、吉南、遼寧遼河等地區(qū)。不同地區(qū)的變質(zhì)巖系變質(zhì)程度有較大差異, 總體變質(zhì)較淺, 一般為綠片巖相,局部達(dá)低角閃巖相至高角閃巖相。

阜平地區(qū)從原阜平雜巖中分出的古元古代的灣子群主要由泥質(zhì)片巖組成。劉樹文和梁海華(1997)通過對(duì)平山西柏坡出露的石榴十字片巖、石榴鋁直閃石片麻巖和夕線二云鉀長(zhǎng)片麻巖的研究, 將其變質(zhì)演化分為三個(gè)階段, 早期礦物組合為Grt+Tau+Pl+Mus+Bt+Rut+Qtz+Kfs, 形成的溫壓條件為T=680℃左右, p=0.82 GPa; 中期的礦物組合為Grt+鋁直閃石+Bt+Pl+鈦鐵礦+剛玉+Sil(毛發(fā)狀)+Qtz+Kfs+Mus, 形成的溫度在690～800℃區(qū)間,壓力在0.65～0.80 GPa區(qū)間; 晚期礦物組合為鐵尖晶石+Kfs+Sil(針柱狀), 形成溫度T=650～750℃, 壓力p＜0.65 GPa; 組成一條順時(shí)針的p-T軌跡。

贊皇地區(qū)的古元古代官都群和甘陶河群為一套淺變質(zhì)沉積巖系, 變質(zhì)程度僅為綠片巖相。

中條地區(qū)的絳縣群是一套變質(zhì)的中基性火山沉積建造, 總體經(jīng)歷了高綠片巖相-低角閃巖相的變質(zhì)改造, 角閃巖相變質(zhì)的溫壓條件為T=510℃, p= 0.38 GPa(孫大中和胡維興, 1993)。中條群原巖為泥砂質(zhì)-碳酸鹽巖沉積建造, 經(jīng)歷了與絳縣群相似的變質(zhì)作用, 但變質(zhì)程度更低, 主體為綠片巖相。梅華林(1994)曾對(duì)絳縣群橫嶺關(guān)組和中條群篦子溝組的泥質(zhì)巖石進(jìn)行了變質(zhì)作用研究, 變質(zhì)演化具有順時(shí)針p-T軌跡型式(圖8)。

圖8 中條地區(qū)古元古代絳縣群和中條群變泥質(zhì)巖石的變質(zhì)演化p-T軌跡(據(jù)梅華林, 1994)Fig. 8 The metamorphic p-T path of pelitic rocks in Paleoproterozoic Jiangxian Group and Zhongtiao Group, Zhongtiao region (after MEI et al., 1994)

呂梁地區(qū)的界河口群以碎屑巖-碳酸鹽巖為主,夾少量基性火山巖, 總體經(jīng)歷了角閃巖相的變質(zhì)改造。呂梁群為一套含條帶狀鐵硅質(zhì)建造的濱海-淺海陸源碎屑-火山巖建造。據(jù)盧保奇等(2003)研究, 在山西婁煩存在由低綠片巖相到低角閃巖相的遞增變質(zhì)帶, 由北向南依次為綠泥石帶、黑云母帶、鐵鋁榴石帶、十字石-藍(lán)晶石帶和紅柱石-夕線石帶, 該變質(zhì)帶的北部和南部分處于不同的變質(zhì)條件, 北部以中壓變質(zhì)作用為主(p=0.3～0.7 GPa), 而南部以高溫低壓變質(zhì)為主(T=600℃)。遞增變質(zhì)帶的形成和發(fā)展受西川河韌性剪切斷裂帶控制。于津海等(1999)在該地區(qū)研究時(shí), 也證實(shí)了藍(lán)晶石的存在, 并認(rèn)為紅柱石最早形成, 而后形成了十字石、藍(lán)晶石和石榴石等礦物組合, 而夕線石形成最晚, 所以不應(yīng)將紅柱石(假象)單獨(dú)劃分出一個(gè)與夕線石并列的變質(zhì)帶, 紅柱石的特征屬于接觸變質(zhì)成因。于津海等(1999)還指出, 呂梁群曾遭受兩期區(qū)域變質(zhì), 早期為動(dòng)力變質(zhì)為主,呈南北向分布, 變質(zhì)程度僅為低綠片巖相。第二次區(qū)域變質(zhì)形成南北向分布的遞增變質(zhì)帶。現(xiàn)將呂梁群和阜平地區(qū)灣子群的富鋁片麻巖的變質(zhì)演化p-T軌跡列于圖9。中條山前寒武紀(jì)的變質(zhì)巖的變質(zhì)時(shí)代為1 885～1 850 Ma(劉樹文等, 2007), 呂梁山變質(zhì)巖的變質(zhì)時(shí)代為1 890～1 870 Ma(Trap et al., 2009)。

呂梁地區(qū)還分布有較呂梁群更新的一些古元古代地層, 如嵐縣群、野雞山群和黑茶山群等。嵐縣群是一套陸源碎屑巖-碳酸鹽巖建造, 野雞山群為一套陸源碎屑巖-火山巖建造。這兩個(gè)群均已遭受低綠片巖相-高綠片巖相變質(zhì)改造。黑茶山群為磨拉石建造, 分布局限, 僅受到低綠片巖相變質(zhì)改造。河南嵩山地區(qū)的嵩山群為一套泥砂質(zhì)碎屑巖組合,變質(zhì)程度僅為低綠片巖相。五臺(tái)山地區(qū)的滹沱群分布于五臺(tái)群南側(cè), 不整合于五臺(tái)群之上, 主要變質(zhì)巖石類型有變質(zhì)礫巖、變質(zhì)砂巖、變質(zhì)砂板巖、千枚巖、結(jié)晶碳酸鹽巖和變質(zhì)基性火山巖。典型的變質(zhì)礦物組合有: Ser+Chl+Qtz+Pl(富鈉)、Pl(富鈉)+Act+Ep±Qtz。根據(jù)Ser-Chl礦物對(duì)計(jì)算的變質(zhì)溫度為270～370℃, 根據(jù)白云母b0值計(jì)算的變質(zhì)壓力為0.51～0.81 GPa, 屬于高壓型綠片巖相變質(zhì)(黨修鵬, 1993)。

圖9 呂梁地區(qū)古元古代斜長(zhǎng)角閃巖(a)及阜平地區(qū)灣子群富鋁片麻巖(b)的p-T軌跡Fig. 9 The p-T paths of Paleoproterozoic amphibolite from Lüliang region (a) and rich-Al gneiss from Wanzi group, Fuping region (b)

吉南地區(qū)的老嶺群和集安群以及遼寧地區(qū)的遼河群是古元古代淺變質(zhì)巖系的重要代表。

邵建波等(1995)利用石榴子石成分環(huán)帶反演構(gòu)建了集安群泥質(zhì)變質(zhì)巖的變質(zhì)演化軌跡。認(rèn)為軌跡反映了兩個(gè)階段的變質(zhì)演化過程, 早期是逆時(shí)針的演化軌跡, 晚期是順時(shí)針的演化軌跡, 說明兩個(gè)階段的變質(zhì)作用發(fā)生于不同的構(gòu)造演化階段。

賀高品和葉慧文(1998a, b)對(duì)遼寧的遼河群和吉南的老嶺群、集安群研究后提出: 北遼河群和老嶺群可合稱為遼北變質(zhì)地體, 變質(zhì)程度達(dá)中壓低角閃巖相, 變質(zhì)演化的p-T軌跡為順時(shí)針型, 其形成與推覆構(gòu)造產(chǎn)生的構(gòu)造增壓有關(guān); 南遼河群和集安群可合稱為遼南變質(zhì)地體, 變質(zhì)程度為低壓高角閃巖相, 變質(zhì)演化的p-T軌跡屬逆時(shí)針型, 與巖漿增溫作用有關(guān)。

郭偉靜和郭洪芳(2006)應(yīng)用p-T-t理論再認(rèn)識(shí)遼河群的變質(zhì)作用。他們根據(jù)紅柱石、堇青石和夕線石的空間分布特征, 將遼河群劃分為中壓相系和低壓相系兩部分, 北側(cè)為中壓相系具有遞增變質(zhì)帶,南側(cè)為低壓相系。北側(cè)中壓相系分布區(qū)自北而南劃分出黑云母帶、石榴子石帶、十字石帶和藍(lán)晶石帶,呈現(xiàn)遞增變質(zhì)帶的特點(diǎn)。

黑云母帶位于中壓相系的北部地區(qū), 分布于下達(dá)河—田師傅—木盂子一帶, 主要變質(zhì)礦物組合為Mus+Qta+Bt±Chl, Pl+Bt+Qtz+Mus;

石榴子石帶分布于海城市—草河掌—八里甸子一帶, 主要變質(zhì)礦物組合為Bt+Mus+Alm+Qtz, Bt+Mus+Alm+Pl+Qtz, Bt+Alm+Pl+Qtz, Alm+Bt+Pl+ Mic+Qtz和Mus+Bt+ Chl+Alm+Pl+Qtz;

十字石帶分布于吉洞峪—賽馬一帶, 主要變質(zhì)礦物組合為Bt+Mus+Pl+St+Alm+Qtz, Bt+Pl+ St+Alm+Qtz和Bt+St+Qtz+Alm;

藍(lán)晶石帶分布于青石嶺—青城子一帶, 主要變質(zhì)礦物組合為St+Ky+Bt+Alm+Qtz±Pl和St+Ky+Bt+Qtz±Alm±Mus。

郭偉靜和郭洪芳(2006)認(rèn)為不同級(jí)別的礦物組合均為變質(zhì)作用峰期的產(chǎn)物, 因而不同意賀高品等(1998a, b)在劃分變質(zhì)階段的基礎(chǔ)上計(jì)算出的每個(gè)變質(zhì)階段礦物組合形成的溫度壓力數(shù)據(jù)。并且認(rèn)為變質(zhì)作用是一個(gè)連續(xù)演化的過程, 不宜劃分階段,礦物組合反映的變質(zhì)級(jí)別差異可能代表變質(zhì)時(shí)不同部位的埋深不同。總之, 他們認(rèn)為遼河群北部中壓相系的礦物組合是大陸碰撞造山帶變質(zhì)作用常見的情況, 南部出現(xiàn)低壓相系的礦物組合則與大陸碰撞造山帶中產(chǎn)生的熔融體的加熱作用有關(guān)。據(jù)Li等(2006)的研究, 遼吉花崗巖和南北遼河群具有相同的εNd值, 嚴(yán)格限于0到2, 說明它們具有相似的物源, 并且遼吉花崗巖與伴生的南北遼河群具有相似的Nd模式年齡(TDm從2.4 Ga到2.6 Ga), 說明二者基本同時(shí)形成, 它們形成于同一個(gè)大陸塊體在古元古代形成的裂谷環(huán)境。趙國春(2009)根據(jù)粉子山群(Zhao未刊資料)、北遼河群(賀高品等, 1998b; 李三忠等, 2001)、老嶺群(賀高品等, 1998b)所測(cè)得的順時(shí)針p-T軌跡以及荊山群(盧良兆等, 1996)、南遼河群和集安群(賀高品等, 1998b; 李三忠等, 2001)所測(cè)得的逆時(shí)針變質(zhì)演化軌跡(詳見圖10), 認(rèn)為兩種形式的p-T軌跡構(gòu)成了雙變質(zhì)帶。從上可知, 該區(qū)變質(zhì)演化p-T軌跡和形成的大地構(gòu)造環(huán)境尚存在不同認(rèn)識(shí), 需進(jìn)一步加以研究。

這些古元古代巖群的沉積時(shí)代大致在2 100 Ma左右, 變質(zhì)時(shí)代大體發(fā)生在1.85 Ga左右。

圖10 膠—遼—吉古元古代變質(zhì)巖帶中變質(zhì)作用演化的p-T軌跡(據(jù)Zhao et al., 2012)Fig. 10 The p-T paths of metamorphic evolution of Paleoproterozoic Jiao–Liao–Ji metamorphic belt (after Zhao et al., 2012)

6 華北克拉通變質(zhì)作用演化

總的看來, 華北克拉通的變質(zhì)作用演化可以從時(shí)間尺度和空間分布尺度理出以下脈絡(luò)。

就時(shí)間尺度而言, 分布于鞍山—本溪地區(qū)的古—中太古代表殼巖已遭受角閃巖相變質(zhì)改造, 由于分布局限, 加之研究程度不夠, 尚缺乏變質(zhì)年齡數(shù)據(jù)。但在鞍山地區(qū)3.77 Ga條帶狀?yuàn)W長(zhǎng)花崗巖中獲得了3 560 Ma的變質(zhì)年齡, 在中太古代片麻巖中獲得了3.0～3.3 Ga的變質(zhì)年齡。這些數(shù)據(jù)表明華北克拉通曾在古—中太古代期間發(fā)生過區(qū)域變質(zhì)作用,這對(duì)于認(rèn)識(shí)華北克拉通的早期演化具有重要的意義。

在河南魯山的太華雜巖中形成于2 845～2 838 Ma的斜長(zhǎng)角閃巖中獲得第一期為2 776 ～2 792 Ma、第二期為2 671～2 651 Ma的變質(zhì)年齡, 在形成于2 832～2 829 Ma的TTG巖系中獲得了2 772 Ma的變質(zhì)年齡(Liu et al., 2009)。在山東沂水地區(qū)新太古代麻粒巖-TTG組合的麻粒巖中碎屑變質(zhì)鋯石獲得了2 715 Ma的變質(zhì)年齡(趙子然等, 2009)。這些數(shù)據(jù)表明至少在河南魯山、魯西等地的中太古代末期—新太古代早期形成的巖系經(jīng)歷了新太古代早期的變質(zhì)改造。

新太古代中晚期及末期, 各微陸塊都共同經(jīng)歷了2.5 Ga左右的變質(zhì)-構(gòu)造-熱事件(翟明國和卞愛國, 2000; Zhai and Liu, 2003)。此期間, 華北克拉通普遍經(jīng)歷了大規(guī)模的TTG巖系侵入, 在2 530～2 450 Ma期間, 以中低壓麻粒巖相變質(zhì)為代表的基底區(qū)域變質(zhì)作用發(fā)生, 呈面狀分布和逆時(shí)針的p-T軌跡特征與克拉通基底的板底墊托或地幔柱上隆有關(guān), 標(biāo)志克拉通的形成。

華北克拉通形成之后在內(nèi)部和邊緣形成了三個(gè)古元古代活動(dòng)帶(翟明國, 2010), 火山-沉積巖大致發(fā)育在2.3～1.95 Ga, 隨著活動(dòng)帶的閉合在1.95～1.90 Ga發(fā)生了區(qū)域變質(zhì)改造, 之后又發(fā)生了強(qiáng)烈的疊加變質(zhì), 表現(xiàn)為1.85～1.80 Ga的麻粒巖相-高角閃巖相的等溫降壓或降溫降壓的疊加變質(zhì), 并在1.80 Ga發(fā)生角閃巖相退變質(zhì)。至少在1.85～1.82 Ga和1.80 Ga的疊加變質(zhì)廣泛發(fā)生于華北克拉通內(nèi)(翟明國, 2010)。

在古元古代的晚期至少發(fā)生兩次區(qū)域變質(zhì)作用, 第一次在1 965～1 900 Ma期間, 由于陸塊之間開始發(fā)生俯沖碰撞或逆沖增壓, 形成中低壓/高壓麻粒巖相變質(zhì)和局部高角閃巖相變質(zhì), 變質(zhì)高峰約在1 950 Ma左右。在1 926～1 900 Ma期間局部發(fā)生超高溫麻粒巖相變質(zhì), 其高峰期在1 923～1 920 Ma間, 與地殼回返、地幔上涌導(dǎo)致的熱流增加有關(guān)。這一階段的變質(zhì)與1 965～1 950 Ma期高峰期變質(zhì)屬同一大變質(zhì)旋回的不同發(fā)展階段。

第二次區(qū)域變質(zhì)作用發(fā)生于1 890～1 800 Ma期間, 代表另一次的大陸俯沖碰撞, 其高峰期在1 860～1 850 Ma之間, 再次發(fā)生中高壓麻粒巖相和角閃巖相變質(zhì), 同時(shí)伴隨有深熔作用和不同程度的重結(jié)晶作用。

我們對(duì)古元古代晚期變質(zhì)事件劃分的認(rèn)識(shí)與Peng等(2014)總結(jié)的華北克拉通1 950～1 850 Ma變質(zhì)事件的時(shí)間分布基本一致, Peng等(2014)進(jìn)一步將該時(shí)間段的變質(zhì)事件劃分為四期: ～1 955 Ma(M1),～1 920 Ma(M2), ～1 885 Ma(M3)和～1 850 Ma(M4),并與西部陸塊的形成、東部陸塊的形成以及東西兩陸塊的碰撞連接相聯(lián)系。

演化到中元古代, 變質(zhì)作用已很微弱, 僅見于華北克拉通北緣的裂谷盆地, 變質(zhì)作用很低, 僅為低綠片巖相。

從空間尺度看, 面狀分布的中低壓麻粒巖相變質(zhì)作用主要分布于華北克拉通北中部太古宙晚期的基底巖系中, 與大面積的TTG巖系伴生, 由于大量巖漿的侵位, 區(qū)域熱流值高呈面狀分布。只古元古代中晚期在不同的造山帶, 變質(zhì)巖系呈帶狀分布,在靠近島弧外側(cè)可以出現(xiàn)中高壓的變質(zhì)巖系, 變質(zhì)程度可以達(dá)到麻粒巖相-高角閃巖相, 在靠近大陸一側(cè)變質(zhì)程度較淺, 多為綠片巖相-角閃巖相, 如果有大量花崗質(zhì)巖石伴生, 可以出現(xiàn)遞增變質(zhì)帶, 變質(zhì)級(jí)別可以達(dá)到高角閃巖相。在靠近俯沖帶由于板片拆沉導(dǎo)致地幔上涌, 局部可以出現(xiàn)超高溫變質(zhì)作用。由于高壓麻粒巖和超高溫麻粒巖一般位于俯沖帶附近, 因此它們一般呈帶狀分布。

Acknowledgements:

This study was supported by China Geological Survey (No. 1212010811048).

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Constituents and Evolution of the Metamorphic Basement of the North China Craton

SHEN Qi-han, GENG Yuan-sheng, SONG Hui-xia
Institute of Geology, Chinese Academy of Geological Sciences, Beijing 100037

Precambrian metamorphic basement of North China Craton (NCC) is composed of five sets of different types of metamorphic rocks. In the formation process, the NCC experienced multiple tectonic activities, multiple magma emplacement, multiple metamorphism, different degrees of migmatization and anatexis. The rocks suffered multiple superposition of different geological processes and, therefore, the NCC has a complicated evolution history. From Archean to Late Paleoproterozoic, the NCC mainly underwent five stages of regional metamorphism. Anshan area experienced amphibolite facies metamorphism in Paleo/Meso-Archean. However, no metamorphic ages have been obtained except 3 560 Ma and 3 000～3 300 Ma metamorphic ages obtained from TTG series. In Lushan Taihua complex of Henan, 2 776～2 792 Ma and 2 671～2 651 Ma metamorphic ages are obtained from Mesoarchean amphibolites, which represent metamorphism in early Neoarchean. Granulites-TTGseries and granite-greenstone belt of Neoarchean both experienced metamorphic transformation in late Neoarchean and early Paleoproterozoic. In Paleoproterozoic, on the northern margin of the NCC, L-MP/HP granulite facies metamorphism occurred between 1 965～1 900 Ma and UHT metamorphism appeared locally. This metamorphism is considered to be related to the continental collision and subsequent mantle upwelling. In Late Paleoproterozoic (1 890～1 800 Ma), in the central and eastern NCC, high-pressure granulite facies to amphibolite facies metamorphism occurred in Jiao–Liao–Ji belt, which indicates the collision and collage of continental blocks. Different types of metamorphic rock series experienced different kinds of metamorphism, which reflect different tectonic settings. A large number of late Archean TTG rock series and planar distribution M-LP granulites are mainly located in the central-northern part of NCC. They generally have counterclockwise p-T paths, which reflect mantle plume underplating tectonic setting. Granite-greenstone series of Neoarchean experienced a metamorphism in late Neoarhcean and early Paleoproterozoic with clockwise p-T paths, reflecting a compound tectonic setting of back-arc and mantle plume. Two metamorphic events that occurred in the Late Paleoproterozoic formed high-pressure granulite facies with clockwise p-T paths, reflecting the collision and collage of continental blocks, which means that plate tectonics system similar to Phanerozoic had appeared.

North China Craton; M-LP/HP/UHT metamorphism; mantle plume underplating; p-T paths; collision and collage

P544.1; P542.4

A

10.3975/cagsb.2016.04.02

本文由中國地質(zhì)調(diào)查局工作項(xiàng)目(編號(hào): 1212010811048)資助。

2016-03-04; 改回日期: 2016-05-12。責(zé)任編輯: 閆立娟。

沈其韓, 男, 1922年生。研究員, 中國科學(xué)院院士。主要從事變質(zhì)巖和前寒武紀(jì)地質(zhì)研究。電話: 010-68999660。E-mail: huixiasong@cags.ac.cn。