由蘭陽平原鑽井岩心沉積層的沉積環境、沉積層序分析和地殼變動速率分析 的結果，有下列幾點看法：
一.末次冰期以來的環境變遷，23000-18000 yr BP 為低海水位時期，現今平原區 海岸線東側應有一障壁沙洲阻隔波浪作用營力，故平原內部沼澤區分布廣泛，而 平原陸側則屬於辮狀河環境，南北兩側分布小範圍沖積扇環境或為岩盤無沉積物 覆蓋。18000-9000 yr BP 為海進時期障壁沙洲向西(陸側)遷移，沿海區域快速變 深為上遠濱，沼澤的分布區域快速變小，辮狀河沉積前緣向上游後退，山麓邊緣
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三.蘭陽平原張裂盆地與南區和北區的邊界分別為濁水斷層(牛鬥斷層)和礁溪斷 層。利用山麓邊緣岩芯資料推論濁水斷層屬於中央山脈和雪山山脈的界線斷層，
是牛鬥斷層在平原內部的延伸。頭城和竹安地區之間的沉降速率呈現顯著差異，
兩地區之間必然有一邊界造成南北兩側沉陷速率不同，本文將此邊界命名為礁溪 斷層，由頭城和竹安之間向西南延伸至平原西側與牛鬥斷層相接。蘭陽平原張裂 盆地位於主要沉陷區，東側陷落較快，並以沉陷核心為軸沉陷速率向南北兩側邊 界遞減，且陷落速率南北對稱，本研究推測此張裂盆地屬於地塹陷落形成的盆地，
為沖繩海槽向西擴張所造成。
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詹新甫(1976)台灣雪山山脈之摺皺與塊體運動，台灣省地質調查所彙刊，第二十 五號，第29-34頁。
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蔡義本(1976)宜蘭地區之地震研究，礦業技術第14卷，第5期，第156-165頁。
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